저작자표시-비영리-변경금지 2.0 대한민국

이용자는 아래의 조건을 따르는 경우에 한하여 자유롭게

l 이 저작물을 복제, 배포, 전송, 전시, 공연 및 방송할 수 있습니다.

다음과 같은 조건을 따라야 합니다:

l 귀하는, 이 저작물의 재이용이나 배포의 경우, 이 저작물에 적용된 이용허락조건을 명확하게 나타내어야 합니다.

l 저작권자로부터 별도의 허가를 받으면 이러한 조건들은 적용되지 않습니다.

저작권법에 따른 이용자의 권리는 위의 내용에 의하여 영향을 받지 않습니다.

이것은 이용허락규약(Legal Code)을 이해하기 쉽게 요약한 것입니다.

Disclaimer

저작자표시. 귀하는 원저작자를 표시하여야 합니다.

비영리. 귀하는 이 저작물을 영리 목적으로 이용할 수 없습니다.

변경금지. 귀하는 이 저작물을 개작, 변형 또는 가공할 수 없습니다.

http://creativecommons.org/licenses/by-nc-nd/2.0/kr/legalcodehttp://creativecommons.org/licenses/by-nc-nd/2.0/kr/

이학석사 학위논문

Mineralogy and Geochemistry of granitic

pegmatite, Lichenhills, Outback Nunatak,

North Victoria land, Antarctica

남극 북빅토리아 랜드, 라이켄 힐즈, 아웃백 누나탁

지역의 화강암질 페그마타이트의 광물학적 지구화학적

연구

2017년 2월

서울대학교 대학원

지구환경과학부

김 태 우

i

Abstract

Mineralogy and Geochemistry of granitic

pegmatite, Lichen hills, Outback Nunatak,

North Victoria land, Antarctica

Taewoo Kim

School of Earth and Environmental Sciences

The Graduate School

Seoul National University

Pegmatite is Macrocrystalline rock and composition of rock

forming minerals is similar to granite. Tourmaline is boron-rich

mineral which is much content in pegmatite. General chemical

formula is XY3Z6Si6B3O27(OH,O,F)4. Tourmaline have useful

information about the environment and conditions of deposition.

ii

And significance of petrogenetic indicator recently has gained

more attention. Besides, variability in its crystal-chemistry

reflects physical and chemical changes during

crystallization.(Henry and Guidotti et al., 1985; Jolliff et al., 1986).

The study area is located in Lichen hills and Outback Nunatak,

North Victoria land, Antarctica. Lichenhills rocks are composed of

granitoids, leucogranites and dolerites. Outback nunatak rocks are

composed of granitic pegmatite and Precambrian schist. So,

Igneous rocks of Outback Nunatak and igneous rock of Lichenhills

are from same Granite habour Intrusive, but origin is little bit

different. Lichen hills' rocks are more close to S-type rather than

Outback nunatak’s. In Outback nunatak’s pegamatie, tourmaline

is well discovered. Due to chemical difference, zoning is well

developed on 001 side of macrocrystalline tourmaline. These

tourmalines belong to schorl-elbaite solid solution and which

indicate that Li, Mg contents is poor, Al, Fe contents is abundant

iii

when tourmaline were formed. Ferrischorl (ferric

oxide)substitution (Fe3+Al-1) from core to rim occur. This

means oxidation state of hydrothermal fluid increase at late period

making rim of tourmaline. This can be done by mixture of

hydrothermal fluid or supergene water which is more oxidizing

fluid or boiling of hydrothermal fluid,

Keywords : pegmatite, tourmaline, petrogenetic indicator, S-type,

chemical zoning, schorl-elbate, ferrischorl substitution

Student Number : 2014 - 20326

iv

Table of Contents

Abstract i

Table of Contents ................................................................................ iv

List of Figures ....................................................................................... v

List of Tables ....................................................................................... ix

1. Introduction ....................................................................................... 1

2. Geological Setting & Sample information ..................................... 3

3. Method ................................................................................................ 6

4. Result and Discussion

4.1 Macroscopy & Microscope observation ..................................... 9

4.2 Chemical composition ................................................................. 12

4.3 Tourmaline observation ............................................................... 17

4.4 Tourmaline geochemistry............................................................ 19

5. Conclusion ....................................................................................... 24

6. Reference ........................................................................................ 27

Figures, Tables .................................................................................... 28

Abstract in Korean ............................................................................ 86

v

List of Figures

Figure 1. Overall map of Antarctica and Location of Northern

Victoria land, Antarctica (after Woo et al ., 2013)

Figure 2. Three tectonic terranes of the Northern Victoria Land

(Capponi et al., 1999a)

Figure 3. General stratigraphy of the Beacon Supergroup in the

Central Transantartic in North Victoria Land.

Stratigraphic units are formations.

Figure 4. Geological map of Outback Nunatak and Lichenhills of

Northern Victoria Land (prepared by the ganovex-team)

Figure 5. Granitoids from Lichenhills

Figure 6. Thin section images of Lichenhills granitoids

Figure 7. Leucogranite from Lichenhills

Figure 8. Thin section images of leucogranite from Lichenhills

vi

Figure 9. Dolerite from Lichenhills

Figure 10. Thin section images of dolerite from Lichenhills

Figure 11. Granitic pegmatite from Outback Nunatak

Figure 12. Thin section images of granitic pegmatite from Outback

Nunatak

Figure 13. Metamorphic rocks from Outback Nunatak

Figure 14. Thin section images of metamorphic rocks from Outback

Nunatak

Figure 15. Classification of igneous rocks by the normative

Quartz(Q)-Alkalifeldspar(A)-Plagioclase(P) diagram

(After Streckeisen, 1976)

Figure 16. Classification of igneous rocks by normative Or-An-

Ab(After Streckeisen, 1976)

Figure 17. SiO2 VS molar Al2O3/(Na2O+CaO+K2O) ratio.

Figure 18. ACF diagram (After Hine et al, 1987)

Figure 19. A'KF diagram

vii

Figure 20. Ternary diagram of Rb-Sr-Ba (after Biste, 1978). The

arrow represents the differentiation trend.

Figure 21. Y vs Nb tectonic discriminant diagram (ppm)

Figure 22. Yb vs Ta tectonic discriminant diagram (ppm)

Figure23. Rb-(Y-Nb) and Rb-(Yb+Ta) discriminant diagrams

Figure 24. Cl chondrite Normalized REE pattern

Figure 25. Primitive mantle Normalized spider diagram

Figure 26. Tourmaline observed by microscope

Figure 27. BSE image of Tourmaline

Figure 28. Common tourmaline end member and Triangular diagram

showing (Henry and Guidotti, 1985)

Figure 29. Al-Fe(tot)-Mg diagram ( in molecular proportions) for

tourmalines from Outback Nunatak rocks. (After Henry

and Guidotti, 1985 and Plimer and Lees, 1988).

Figure 30. Ca-Fe(tot)-Mg diagram (in molecular proportions) for

viii

tourmalines from Outback Nunatak rocks. (After Henry

and Guidotti, 1985 and Plimer and Lees, 1988).

Figure 31. Plots of cation occupancies of tourmaline from Outback

Nunatak.

Figure 32. Plots of cation occupancies of tourmaline from Outback

Nunatak

ix

List of Tables

Table 1. Simplified, general stratigraphy of the Northern Victoria

Land (Woo et al., 2103)

Table 2. XRF data, norm analysis in Lichenhills and Outback

Nunatak

Table 3. ICP-MA data, in Lichenhills and Outback Nunatak

Table 4. Microprobe analyses of colored zones of tourmalines from

Outback Nunatak

1

1. Introduction

Pegmatite is Macrocrystalline rock and composition of rock forming

minerals is similar to granite. Particle size of granitic pegmatite is

from 2.5cm to 30cm. These granitic pegmatites have various origins

and can show a similarly varied range of rare-element enrichment(e.

g Li, Cs, Ta, Nb, Rb, Y, REE, Sc, U, Sn, F, b, Be) (T. Scott Ercit et al,,

2005).

Tourmaline is boron-rich mineral which is much content in pegmatite.

General chemical formula is XY3Z6Si6B3O27(OH,O,F)4. These

tourmaline composed of major elements such as Si, Mg, Ca, Fe, Al, Mn

and minor elements such as Li, F, B. Tourmaline have useful

information about the environment and conditions of deposition. And

significance of petrogenetic indicator recently has gained more

attention. Besides, variability in its crystal-chemistry reflects

physical and chemical changes during crystallization (Henry and

Guidotti et al., 1985; Jolliff et al., 1986).

The study area is located in Lichen hills and Outback Nunatak, North

Victoria land, Antarctica. According to study of Zeller and Dreschhoff

(1990), it is reported that radioactivity value in Lichen hills in Victoria

land is very high. For these reason, rock samples of these area are

2

collected at first. But because its weather and ground condition is s

severe, samples are obtained only few from outcrop. The number of

samples is 15 in Lichen hills, 7 in Outback Nunatak. Even though the

number of samples is small, it is worthy to study because the samples

are from Antarctic which isn’t studied much. Granitic pegmatites from

these two area are related Granite Habour Intrusive. But among this

rock samples, tourmalines from Outback Nunatak are observed very

easily contrary to samples from Lichenhills.

So, purpose of this study is ; (1) to know basic information of these

two region’s lithofacies by Microscope observation and major and

minor element analysis. (2) to find out tectonic setting when these

two regions were formed (3) to find out difference of these two

region's environment when Granite habour Intrusive intrude. If

exploration will be done this region, purpose of this study is to provide

basic guideline and base data in these regions. For mineralogical study,

observation using microscope and SEM-EDS is conducted. For

geochemical analysis, major element, minor element, REE contents of

whole rock are analyzed by XRF, ICP-MS. For tourmaline analysis,

EPAM analysis is conducted for each grain from core to rim.

3

2. Geological Setting

North Victoria land in Antarctica is located in end of

TAM(Transantarctic Mountains), side of the Pacific Ocean )(Woo et

al.,2013)(Fig.1). This area has very good condition to study geology

because rocks are exposed very widely in Antarctica. Stratigraphic

sequence of TAM(Transantarctic Mountain) and Vitoria land is

represented that ; metasedimentary rocks and metamorphic rocks of

Precambrian-early Cambrian, shallow and deep-marine siliciclastics

and shallow-marine carbonates, and volcanics of Cambrian-

Ordovician, dolerite, basalts, volcaniclastics and fluvial sandstone of

Devonian-Cenozoic, volcanics and glacial deposits of

Jurassic.(Table.1) Progress of Tectonic setting of

TAM(Transantarctic Mountain) and Victoria island is divided into 3

stages. First, Ross orogeny took place from neo-proterozoic to

early-paleozoic. Terrain of North Victoria land consist of 3

accretionary terrain; Wilson Terrain, Bowers Terrane, Roberton Bay

Terrane. (Capponi et al., 1999a) (Fig.2). Wilson Terrain consist of

metamorphic rocks undergone medium-high metamorphism of

neoproterozoic-early-paleozoic and Granite Harbour Intrusives

which are calc-alkali plutons intruded from Cambrian to Ordovician

4

(Stump el al., 1995). Second stage after Ross orogeny is silent

tectonic period which is from late-Paleozoic to Jurassic. In this

stage, Ross orogenic zone became plain bed rock after it was eroded

in a wide range. On basement rock, Beacon Supergroup consisting of

silicate clastic sediment is piled up. Beacon Supergroup consist of

Taylor Group in Devonian, Victoria Group from late Carboniferous to

early Jurassic, Ferrar Group in mid Jurassic(Fig.3). In North

Victoria land, there is no Taylor Group. In the lowest part of Victoria

Group in North Victoria land, there is diamictite which is glacier

sediment in late Carboniferous. In upper side, there is Takrouna

formation consisting of fluvial deposit in Permian. It mainly consist

of sandstone, coal siltstone, small amount of mudstone. The top part

of Victoria Group is section peak formation in Triassic period, which

consist of medium-coarse grained quartz sandstone(Collinson et al.,

1986). Ferrar Group in North Victoria land consist of pyroclastic

material, kirkpatrick basalt from underneath. It considered to

product of early volcanic activity related with separation of

Gondwanaland(Woo et al., 2013). 7 Samples are selected in Outback

Nunatak, 15 samples are selected in Lichenhills in Wilson tarrane.

Lithofacies of Outback Nunatak's outcrop are composed of

5

GHI(Granit harbor intrusives from ordovician, wsr(rennick schist)

from precambrian mainly, gbs(beacon supergroup:light coloured ,

quartztic to arkosic sandstones, minor quartz conglomerates),

gfd(ferrar supergroup:ferrar dolerite) little from upper paleozoic to

mesozoic. Lithofacies of Lichenhills' outcrop are GHI(Granite

harbour intrusives) from ordovician, gfd(ferrar supergroup : ferrar

dolerite) and gbs(beacon supergroup:light coloured , quartztic to

arkosic sandstones, minor quartz conglomerates) from upper

paleozoic to mesozoic along the sub- beacon erosion surface (Fig.4).

To sum up, in Outback Nunatak there are metamorphic complex in

Wilson Group and Granite Harbour Igneous complex, in Lichen hills,

there are and Granite Harbour Igneous complex and dolerite, basalts,

volcanicclastics in Beacon Supergroup, Ferrar Supergroup mainly.

6

3. Method

Total 22 sample of outcrop rock were collected. 7 samples are

collected in Outback Nunatak, 15 samples are collected in

Lichenhills of Wilson tarrane. For petrography, macroscopy and

microscopy are conducted. Thin-sections are made for

microscope observation. To distinguish which mineral is contained

in sample, microscope observation is conducted. If minerals cannot

be distinguished, SEM-EDS is used for that. SEM-EDS can offer

approximate chemical composition of point of thin sections. By

macroscopy and microscopy, it is found that collected samples are

correspond to rock facies investigated geology setting. For major

and minor element analyses, XRF(x-ray Fluorescence

Spectrometer) and ICP-MS was performed by National Center for

Inter-University Research Facilities (NCIRF) at Seoul National

University (SNU), Seoul. Rocks are smashed to 200 mash powder

for obtaining bulk composition. Shimadzu XRF-1700 X-ray

fluorescence (XRF) spectrometer was used to perform major

elements analysis. SiO2, Al2O3, TiO2, Fe2O3, K2O, Na2O, CaO, MgO,

MnO, and P2O5 concentrated of each sample were obtained. All

elements’ standard is rock-based standard. Trace and rare earth

7

element concentrations of samples will be analyzed by Elan 6100

Inductively Coupled Plasma Mass Spectrometer (ICP-MS). By

ICP-MS, REE like lanthanoids(La~Lu) and HFHE(High Field

Strength Element)(Ta, Nb, Hf, Zr, U, Th), LILE(Large Ion

Lithophile Elements)(Yb, Ce, Sr, Ba, Rb) are analyzed. From XRF

data, it can be done to classify rock facies. Also relation between

each major element versus SiO2 in each rock are obtained. From

ICP-MS data, it can be obtained about differentiation trend from

Rb-Sr-Ba and relation of each element versus SiO2 and trend of

REE pattern using Cl Chondrite(MaDonough et al., 1995). Among

these rocks, tourmalines in Outback Nunatak rocks are discovered

more than granite of Lichenhills rocks. In this tourmaline, chemical

zoning is discovered well. Because of chemical composition,

chemical zoning exist. To examine this, SEM-BSE(back scattered

image) image is used. To know chemical difference from core to

rim, electrone probe X-ray microanalyzer analysis (EPMA) is

conducted. Electrone probe X-ray microanalyzer analysis(EPMA)

is performed by SHIMADZU 1610 in KBSI(Korea Basic Science

Institute). Condition of analysis is Acc.V : 15kV, B.C(Beam

Current) : 20nA , B.S(Beam Size) : 1㎛. This was used to perform

8

major elements analysis; SiO2, Al2O3, TiO2, Fe2O3 , K2O, Na2O, CaO,

MgO, MnO, and ZnO of each point. Among samples of Outback

Nunatak, I selected 4 samples which are granite pegmatite having

tourmaline and conducted analysis of 3, 3, 2, 6 tourmaline grains in

each samples. From this analysis, tourmalines are classified and

can be found chemical exchange using exchange vector. By

chemical difference from core to rim, environmental condition of

petrogenesis is interpreted.

9

4. Result and Discussion

4.1 Macroscopy & Microscope observation

Samples from Lichenhills are 15. In case of LH1, LH7, LH8 and

LH15, it looks granitoids, have pink color. Grain size is coarse

grain, 2~5mm. Alkali feldspar and biotite are found very well by

naked eyes (Fig.5). Little alkali feldspar or no quartz were

observed in microscopic analysis (Fig.6). LH1 sample is composed

of mainly orthoclase and biotite, few quartz. Also muscovite is

discovered little. So, this sample can be called two mica granite.

Grain size is 200~800 μm. LH7 sample is composed of quartz,

orthoclase and biotite. Grain size is 400~600 μm. LH15 sample is

composed of mainly quartz and orthoclase and little muscovite.

Grain size is 400~800 μm.

In case of LH2, LH3, LH4 LH5, LH6 and LH14, it looks like

leucogranite which have light color. It can be found that it have little

mafic mineral and composed of mainly coarse quartz, orthoclase.

10

Some samples have very coarse grain of garnet having dark

color(Fig.7). LH2, LH3 samples are composed of mainly quartz,

orthoclase, muscovite and garnet. Garnet is coarse grain from

600~1200 μm. LH4 , LH5 samples are composed of quartz,

orthoclase, plagioclase, muscovite, garnet. Garnet have smaller size

(100~300 μm) rather than LH2, LH3. LH6 sample is composed of

mainly orthoclase, muscovite, coarse grain of quartz and little biotite.

It can be called two mica granite. LH14 is composed of mainly quartz,

orthoclase, little muscovite (Fig.8).

Last group of Lichenhills is rocks having dark color ; LH9, LH10,

LH11, LH12 (Fig.9). In case of LH9, LH10, grain size is fine

relatively. But LH11, LH12 samples have coarse grain. And, quartz

vein is discovered quartz vein in LH10 sample. When these 4

samples are observed by microscope, pyroxene, quartz and biotite

are mainly composed (Fig.10). These samples have directional

nature of biotite which means that these have light metamorphism.

11

Grain size is 100~200 μm In the case of LH11, it is composed

mainly of quartz, pyroxene, orthoclase, biotite and muscovite. Grain

size is 200~800 μm.

In the case of Outback Nunatak samples, in ON1, ON3, ON5, ON7,

granitic pegmatite is discovered(Fig.11). Grain size is

macrocrystalline. In ON1,ON7 sample, there is granite intruded by

granitic pegmatite. Macrocrystalline quartz, tourmaline, muscovite,

alkali feldspar are observed by naked eyes well. . When these 4

samples are observed by microscope, quartz, alkali feldspar,

tourmaline are mainly composed and little muscovite are discovered

(Fig .12).

ON2, ON4 is dark colored metamorphic rock. It is difficult to

distinguish minerals by naked eyes. Cleavage and foliation is well

developed in rock(Fig.13). When these 4 samples are observed by

microscope, this rocks are mainly composed of quartz, muscovite,

biotite and directional nature is discovered (Fig.14). Compared with

12

geological setting of Outback Nunatak, these rocks are considered

to Precambrian schist.

4.2 Chemical composition

4.2.1 Major Element analysis

For geochemistry of rocks, collected rocks are divided to 4 groups

by sampling area and rock type. Because pegmatites among samples

have many macrocrystalline grains, rocks are smashed and grinded

as big as possible for average chemical composition. With XRF data,

norm analysis is conducted(table 1). Because it is impossible to

calculate content on account of volatile composition, tourmaline and

muscovite isn't calculated, so quartz is calculated little bit high. It is

found that Outback Nunatak granitoids are more felsic than Lichen

hills's granitoids . From collected CIWP norm mineral assemblage,

13

rocks are classified using Strekeisen classification(1979)(Fig.15).

Lichenhills igneous rocks are plotted mainly in monzo granite and

Outback Nunatak igneous rocks are plotted mainly in granodiorite.

But Outback Nunatak looks leucogranite by naked eyes and

micoroscope. This difference is from CIPW norm error. This data

means Lichenhills rocks have more alkali elements than Outback

Nunatak's. Monzo granite calls biotite granite which is identified

Lichenhills's have more biotite in thin sections. According to Or-

An-Ab triangular diagram , Lichen hills igneous rocks are plotted

between granite and quartz monzonite, and Outback Nunatak

igneous rocks are plotted mainly in between granite and trondhjemite.

(Fig.16). Although there is little quartz and albite when these are

observed by microscope, in this diagram these are calculated

somewhat. Because these mineral assemblage are calculated with

chemical data, there may be error compared to actual mineral

assemblage. But it is certain that igneous rocks of Outback nunatak

14

have more quartz and plagioclse than igneous rocks of Lichenhills.

Outback Nunatak's point is sided to albite than Lichen hills's point

meaning they have more content of sodium.

In study of White & Chappel(1992), if Na2O contents are under

3.2 %, Al2O3/Na2O+K2O+CaO is over 1.5, rocks are belonged to S-

type. Igneous rocks of Lichenhills have fewer contents of Na2O and

more contents of Al2O3/Na2O+K2O+CaO than Outback Nunatak's. So,

igneous rocks of Lichenhills are more close to S-type(Fig.17).

Also, in ACF diagram(Hine et al., 1987; Fig.18), Outback Nunatak's

points are plotted around A point rather than Lichenhills's so it is

uncertain that rocks are whether S-type or I type. In AF'K diagram

(Fig.19), rocks are belonged to between pelitic and granites. If rocks

are S type, points are sided into pelitic. Lichen hills'rocks are plotted

almost in pelitic area, but Outback's aren't plotted in pelitic area. So,

Igneous rocks of Outback Nunatak and igneous rock of Lichenhills

are from same Granite habour Intrusive , but origin is little bit

15

different.

4.2.1 Whole rock analysis of trace element & rare earth element

analyses

Trace and rare earth element concentrations of samples will be

analyzed by Elan 6100 Inductively Coupled Plasma Mass

Spectrometer (ICP-MS). The result are shown in table 2.

Rb-Sr-Ba diagram (Biste, 1974) show trend of differentiation.

Rocks of Lichen hills differentiation is normal and shows dispersion

(Fig.20). This means Lichen hills rocks are affected from remelting

and partial melting. And igneous rocks of Outback Nunatak have

strongly differentiated.

Nb-Y tectonic setting diagram is shown. (Pearce et al., 1984;

Fig.21)All samples are plotted in volcanic-arc grantes(VAG) plus

16

syn-collisional granites (sys COLG) area. In Ta-Yb tectonic setting

diagram(Fig.22), almost point are plotted in syn-COLG and others

are plotted in VAG. Rb-Y+Nb, Rb-Y+Ta are shown (Fig.23).

These diagram indicate that rocks are originated from Syn-COLG.

Rare earth elements are classified to 2 groups: Lichen hills granitic

pegmatite, Outback nunatak pegmatite. REE contents is normalized

with Cl Chondrite(Nakamura, 1974). (Fig.24).

Overall, Lichen hills rocks have more REE than Outback Nunakta

rocks. Lichen hills rocks LREE contents have a number of times to

hundreds of times than HREE contents. On the contrary, Outback

nunakta's HREE are little bit higher than LREE. Generally, this is

fixed by partition coefficient between melt and mineral. When

mineral crystallize from melt, LREE goes rich in melt. In the Lichen

hills pattern(Fig.24), LREE are much more enriched than HREE,

displays positive Eu anomalies. On the other contrary, Outback

nunatak samples don’t display tendency like this. Negative Eu

17

anomalies in Lichen hills rocks means plagioclase fractional

crystallization happens much.

Primitive mantle Normalized spider diagram are shown.(Fig.25).

Elements are arranged in the order incompatibility. In these two

diagram, incompatible elements are more enriched than compatible

element. But Outback Nunatka's have little compatible elements.

Lichen hill's shows Ba, Sr anomaly which is related Eu anomaly. It

means plagioclase fractional crystallization happens much. Also it

shows Nb anomaly. It is related with mixture of crust material.

Outback nunatak's shows Zr anomaly.

4.3 Morphology of the examined tourmaline

Igneous rocks of Outback Nunatak and igneous rock or Lichenhills

are from Granite Habour Intrusive. But there is difference between

these two region' rock. Outback Nunatak's rocks are more pegmatic

18

and have tourmaline. Tourmaline is discovered in granitic pegmatite

well. Because it is partial samples, it is difficult to know overall

country rock's situation. On naked eyes, when grain size is big,

crystalline shape is well discovered and show acicular structure.

Tourmaline grain size in ON3, ON5 samples is 1~3cm, other grain

size is similar from 2~5mm. On naked eyes, color of center is dark

green, rim is brown to black. Zoning is well developed on 001 side of

macrocrystallin tourmaline, from core to rim color is getting dark,

some have 1 boundary, others have 2~3 boundary. Grain of ON1 is

too small to observe these things on naked eyes but grain of ON3, 5,

7 are well discovered on naked eyes. Oscillatory fine scale zoning is

also observed. These chemical zoning is well observed in

microscope image. (Fig.26). In microscope, color of core is light blue

to green and color of rim is light brown or olive green. Samples cut

to C-axis vertically show zoning well such as ON1-1, ON1-2, ON5,

ON7 samples. Boundary due to chemical difference show well. ON1

19

samples shows 2 boundaries. But samples of ON3 are show subtle

boundary. It is considered that they are not cut to C-axis vertically.

To know chemical difference, BSE images are taken. (Fig.27). In the

case of ON1 samples, zoning is identified, and ON7 samples are well

observed. On contrary it is difficult to find zoning in ON3, ON5

samples.

4.4 Tourmaline geochemistry

Tourmaline is boron silicate mineral have complex chemical

composition because of various element replacement. General

chemical formula is written in many paper, (Henry et al., 1985; jolliff

et al., 1986; London manning et al., 1995), in this paper chemical

formula of tourmaline is used as XY3Z6Si6B3O27(OH,O,F)4. X site is

polyhedral and mainly composed of Na, also various amount of Ca, K,

Mg. Y site is octahedral site and mainly composed of Mg, Fe2+, Fe3+,

Mn, Cr, Li. Z site is octahedral site and mainly composed of Al. Like

20

this, on each X,Y and Z site, element replacement of cation is broad,

change of chemical composition is very big. So it is general to

indicate tourmaline's chemical composition using end member.(Henry

et al 1985., Jolliff et al 1986, London et al 1995) (Fig.28). Almost

natural tourmalines are solid solution of schorl-dravite or schorl-

elbaite. But there is no solid solution between dravite and elbaite.

(Deer et al. 1962). By Benard et al. (1985) expecially, schorl-

dravite solid solution have typical characteristic of peralumonous

granitic rocks. Boron in magma stage influence correlation with felsic

magma. (Chorlton and Martin., 1987)

When express element replacement of cation, it is general to

express it by exchange vector. EPMA analysis is conducted that

tourmaline cut to C-axis vertically (ON1, ON3, ON5, ON 7). The

number of grains is 14, and total point analysed is 32 (Table3). The

number of cation of analyzed data is calculated by 24.5 oxygen

normalized. Content of SiO2 is 35~38Wt%, has similar range and

content of Al2O3 is 34~36%, show small range. Ratio of Fe/(Fe+Mg)

is 0.75~0.95, has wide range, and ratio of Na/(Na+Ca) is 0.90~0.97,

have relatively high value and narrow range. Result of EPMA

analysis are plotted in Al-Fe-Mg triangular diagram.(Fig.29.)

21

According to this diagram, core and rim part are plotted in Li-poor

granitoids and their associated pegmatite. These tourmaline is close

to schorl, between schorl-elbaite, and have environment of poor Mg,

rich Fe, poor Ca. Also, according to Ca-Fe-Mg triangular diagram

(Henty and Guitotti., 1985), core and rim part are plotted in Li-poor

granitoids and their associated pegmatite and aplites (Fig.30). In this

diagram, it is identify that these are close to schorl of schorl-dravite

solid solution. It is thought that this is affluence from parent rock

having more rich Fe content than Mg content. As I said, zoning is

discovered in tourmaline, zoltan & shout(1984) indicated that reason

of this is in rapid growth, dispersion rate of certain didn’t catch up

crystalline rate. Lofgen(1980) in melt of igneous rock, if rapid

decrease of volatile and rapid change of temperature, zoning is

repeated.

ON 1, 3, 5 have lower Fe/(Fe+Mg) and Na/(Na+Ca) content in rim

than in core generally. ON 7 have little bit higher Fe/(Fe+Mg) and

Na/(Na+Ca) content in rim than in core. These means ON 1, 3, 5

grow toward in environment having little Fe, more Ca and ON 7 is

vice versa.

These three samples show chemical zoning. Figure.31 shows core

22

to rim compositional scans of four tourmaline grains that are cut

perpendicular to their c-axis from differnt types of samples. All

grains have similar variation trends showing relative minor changes

in their Al and Si contents with normally Al > Si. Changes in Na and

Ca contents are also small with Na > Ca. These two element have

tendency of increase to rim. But large inverse changes between Fe

and Mg exist for all tourmalines, which may indicate that the fluids

responsible for tourmaline growth had varying Fe/Mg ratios during

the hydrothermal processes.

In substitution vector (Fig.32) Fe-Mg content in Y is maximum 3

p.f.u(per formula unit). But It shows that contents of core and rim

are under 3 p.f.u line. This means that Al substitute in Y. Plotted

points in left side means this tourmaline close to schorl between

schorl and elbaite solid solution.

If Al entered in Y , another site (i.e., in the X site) have deficiency of

alkali element or hydrogen because of charge balances.(Fig.33). In

fig.33 points of core and rim are plotted near alkali-deficiency

substitution vector [{[X]AlNa}{(Fe,Mg)}-1] and hydrogen-

deficiency substitution vector [[{Z]O}{[Y]OH}-1]. It indicated

that Al contents is abundant when tourmaline were formed. This is

23

appear in tourmaline formed from hydrothermal fluid originated from

magma. (London and Manning, 1995)

During ferrischorl substitution occur from core to rim (Fig.34.), Al

substitute into Fe, {Ca(Fe,Mg)}{NaAl}-1 and opposite of

([X]Al)(Na(Fe,Mg))-1 are occur. This means that chemical

composition of hydrothermal fluid change into environment having

rich-Fe contents. From core to rim, opposite of alkali-deficiency

substitution vector occur, which means Al comes out and alkali

contents come into tourmaline. It can be found that in table3.

Ferrischorl (ferric oxide)substitution Fe3+Al-1 means oxidation

state of hydrothermal fluid increase at late period making rim of

tourmaline. This can be done by mixture of hydrothermal fluid and

supergene water which is more oxidizing fluid or boiling of

hydrothermal fluid, (Jolliff et al 1986; London and Manning , 1995).

In fig.34 Al contents is abundant in the first place. When rim are

made, Al contents decrease little bit, but Al contents is rich still. And

value of Fe/(Fe+Mg) contents is also high. Left side means Al deficit

and right side means Al surplus in Z site. Ferrischorl (ferric

oxide)substitution Fe3+Al-1 occur in Z site.

24

5. Conclusion

Among three terrain in Northern Victoria land, Antarctica, Lichen

hills and Outback Nunatak rocks have Granite Habour Intrusive

intruded in Ross Orogeny. By petrography, Lichen hills samples are

devided into Granite Habour Intrusive and Ferrar dolerite. Outback

Nunatak samples are devided into Granite Habour Intrusive and

Precambrian schist. Although these two area's lithography have

Granite Habour Intrusive, there are characteristic differences.

Lichen hills granitoids are two-mica granite and leucogranite. But

Outback Nunatak granitoids are pegmatic granite and have well-

developed tourmaline. In progress of tourmaline formation, boron

contents are critical factor. By judging litography, it is possible that

precambrian schist is source of boron.

By chemical analysis, Lichen hills rocks show characteristics of S-

type granite. Their Na2O contents is under 3.2% and

Al2O3/Na2O+K2O+CaO is over 1.5. But Outback Nunatak rocks Na2O

contents is over 3.2%. And it is uncertain that it is S-type granite

rather than Lichen hills rocks. By Loiselle and Wones(1979), A-

type granitoid is introduced. Outback nunatak rocks characteristics

are correspond to this ; high SiO2 contents(over 73.81%), high Na

25

contents, low Cr contents, low LILE/HFSE , high Fe/Mg , Zr high.

Judging by these things, whereas Lichen hills Granite Habour

Intrusive are made in brisk period of Ross orogeny, Outback

Nunatak Granite Habour Intrusive intrude in late period of Ross

orogeny; Stable caton rift zone . To guess its environment of last

stage of hydrothermal fluid, tourmalines in Outback Nunatak are

investigated. These fluids have Al-rich, Fe-rich, Mg -poor state at

first, and during crystalliztion progress, Fe contents increase, Al

contents decrese. These means mixture of hydrothermal fluid and

supergene water which is more oxidizing fluid or boiling of

hydrothermal fluid. (London and Manning , 1995). Another reason

why tourmaline exist in only Outback Nunatk's is that Outback

Nunatk's have high-Fe-Mg value. If Fe-Mg value is high, even

though late stage of differentiation, there are much Fe-Mg contents

to make tourmaline. That is, because Outback Nunatak rocks contain

precambrian schist, there is possibility that tourmaline are made by

Fe-Mg contents supplied by schist. In short, granitic pegmatite in

Outback Nunatak are made by intrude of hydrothermal fluid

originated late stage magma.

Although there is no ore mineral discovered, because tourmaline

26

study suggest that Outback Nunatak's formation enviroment having

rich Al, Fe. It is good indicator to find out ore originated from

Igneous.

27

6. Reference

우주선, et al. (2013). "남극 북빅토리아 랜드의 지사와 층서” 지질학회지

49권(1호): 165-179.

Biste. (1979). "Die Anwendung geochemischer indikatoren auf die

Zinn-Hoffigkeit herzyn-ischer Granite in Süd-Sardinien."

Reimer

Capponi,. et al (1999). " Structural history and tectonic evolution of

the boundary between the Wilson and Bowers terranes,

Lanterman Range, northern Victoria Land, Antarctica."

Tectonophysics 312(2): 249-266.

Cerny., et al. (2005). "The classification of granitic pegmatites

revisited." The Canadian Mineralogist 43: 2005-2026.

Chappell, B. W., and A. J. R. White. (1992). " I-and S-type granites in

the Lachlan Fold Belt." Geological Society of America Special

28

Papers 272: 1-26.

Collinson,J.W., et al(2003). "Stratigraphy and petrology of Permian

and Triassic fluvial deposits in Northern Victoria Land,

Antarctica. Antarctic Research." Antarctic Research 46: 211-

242.

Dreschhoff., et al (1990). " Evidence of individual solar proton events

in Antarctic snow.” Solar Physics 127(2): 333-346.

Henry, Darrell J., and Charles V. Guidotti. (1985). "Tourmaline as a

petrogenetic indicator mineral- An example from the

staurolite-grade metapelites of NW Maine." American

mineralogist 70(1): 997-1004.

Jolliff, Bl, J. J. PaPike, and JC LAUL. (1967). "SHEARER CK (1986)

Tourmaline as a recorder of pegmatite evolution: Bob Ingersol

pegmatite, Black Hills, South Dakota." Am. Mineral 71: 472-

500.

29

London., et al. (1948). " Chemical variation and significance of

tourmaline from Southwest England." Economic geology 90(3):

495-519.

Lofgren., et al(1980). "Experimental studies on the dynamic

crystallization of silicate melts." Physics of magmatic processes

487

McDonough, et al. (1995). " The composition of the Earth." Chemical

geology 120(3): 223-253.

Pearce., et al (1984). " Trace element discrimination diagrams for the

tectonic interpretation of granitic rocks." Journal of petrology

25(4): 956-983.

Strekeisen, A .(1979). " Classification and nomenclature of volcanic

rocks, lamprophyres, carbonatites and melilitic rocks." Geology

7: 331-335.

30

Stump, E. (1995). " The Ross Orogen of the Transantarctic

Mountains." Cambridge University Press : 284.

Zoltan Bekassy., et al. (1984). " Prevalence of genitourinary

symptoms in the late menopause." Acta obstetricia et

gynecologica Scandinavica 60(3): 257-260.

31

Fig. 1. (a) Overall map of Antarctica, (b) Location of Northern Victoria land, Antarctica (NVL: Northern Victoria Land, SVL:

Southern Victoria Land, CTAM: Transantarctic Mountains)

32

Table 1. Simplified, general stratigraphy of the Northern Victoria Land (Woo et al., 2103)

33

Fig. 2. Three tectonic terranes of the Northern Victoria Land (Capponi et al.,

1999a)

34

Fig. 3. General stratigraphy of the Beacon Supergroup in the Central Transantartic

in North Victoria Land. Stratigraphic units are formations.

35

Fig. 4. Geological map of Outback Nunatak and Lichenhills of Northern Victoria Land (prepared by the ganovex-team) (GHI:

Granit harbor intrusive, wsr:rennick schist, gbs:beacon supergroup, gfd:ferrar supergroup:ferrar dolerite)

36

Fig. 5. Granitoids from Lichenhills (a: LH1, b: LH7, c: LH8, d: LH15)

37

Fig.6. Thin section images (a, b: LH1, c:LH7, d:LH15)

38

Fig. 7. Leucogranite from Lichenhills (a: LH2, b: LH3, c: LH4, d: LH5, e: LH6, f: LH14)

39

Fig. 8. Thin section images (a: LH2, b: LH3, c: LH4, d: LH5, e: LH6, f: LH14)

40

Fig. 9. Dolerite from Lichenhills. (a: LH9, b; LH10, c: LH11, d: LH12)

41

Fig. 10. Thin section images (a: LH9, b: LH10, c: LH11)

42

Fig. 11. Granitic pegmatite from Outback Nunatak. (a: ON1, b:ON3, c:ON5, d:ON7 )

43

Fig . 12. Thin section images (a: ON1, b: ON1, c: ON3, d: ON5, e: ON7, f: ON7)

44

Fig . 13. Metamorphic rocks from Outback Nunatak. (a: ON2, b: ON4)

45

Fig . 14. Thin section images (a: ON2, b: ON4)

46

Table 2. XRF data, norm analysis in Lichenhills and Outback Nunatak (* : Ferrar dolerite)

sample LH1 LH2 LH3 LH5 LH6 LH7 LH9* LH10* LH11* LH12* LH13-1 LH13-2 LH14

SiO2 71.25 74.23 74.65 74.95 75.89 73.04 55.93 62.03 73.64 74.11 75.28 72.39 72.37

Al2O3 14.45 14.55 14.44 14.88 13.12 13.90 17.78 16.45 9.82 14.54 12.57 13.13 14.15

Fe2O3T 2.32 0.65 0.80 1.03 0.60 1.45 7.40 5.85 7.12 0.67 0.80 2.22 2.04

TiO2 0.30 0.04 0.05 0.05 0.07 0.22 1.28 0.98 0.65 0.04 0.13 0.35 0.05

MnO 0.04 0.02 0.02 0.26 0.03 0.02 0.10 0.09 0.22 0.02 0.02 0.04 0.13

CaO 2.06 2.04 2.30 1.23 1.39 2.14 6.78 5.82 2.35 2.04 2.75 2.51 2.29

MgO 0.55 0.04 0.02 0.11 0.07 0.19 5.20 3.56 2.04 0.03 0.02 0.35 0.02

K2O 5.96 4.79 3.69 4.01 6.08 6.02 3.80 3.01 2.22 4.69 4.07 5.23 4.65

Na2O 2.62 3.28 3.60 3.12 2.42 2.70 0.58 1.34 1.43 3.30 3.11 2.71 3.35

P2O5 0.09 0.11 0.10 0.09 0.08 0.11 0.29 0.24 0.02 0.11 0.02 0.07 0.09

LOI 0.31 0.21 0.20 0.22 0.18 0.07 0.63 0.52 0.40 0.43 1.09 0.89 0.74

total 99.93 99.97 99.86 99.94 99.92 99.85 99.79 99.89 99.89 99.97 99.88 99.89 99.87

Q 28.28 32.71 34.95 38.93 35.70 30.21 16.85 25.65 48.91 32.95 36.92 31.73 30.69

Co 0.16 0.51 0.58 3.37 0.21 1.08 0.99 0.86 0.60 0.00 0.00

Or 35.18 28.29 21.79 23.68 35.90 35.53 22.45 17.79 13.08 27.67 24.04 30.88 27.45

Ab 22.11 27.77 30.46 26.40 20.49 22.79 4.91 11.34 12.05 27.85 26.30 22.95 28.30

An 9.64 9.42 10.75 5.55 6.38 8.05 31.71 27.26 11.50 9.42 8.32 8.19 9.84

Hy 1.36 0.09 0.04 0.27 0.17 12.90 8.83 5.06 0.06

Mt 0.00 0.00 0.68 0.26

Hm 2.32 0.66 0.80 0.56 0.60 1.45 7.42 5.86 7.13 0.67 0.80 2.22 1.86

Ru 0.00 0.00 0.00 0.00

Il 0.08 0.05 0.05 0.10 0.06 0.05 0.22 0.20 0.46 0.05 0.05 0.09 0.10

Ap 0.19 0.24 0.21 0.19 0.17 0.23 0.64 0.54 0.05 0.23 0.05 0.15 0.21

Di 1.00 0.10 1.31 0.10

47

sample ON1-1 ON1-2 ON3 ON7-1 ON7-2

SiO2 77.24 80.20 76.01 75.17 73.13

Al2O3 11.58 11.04 14.29 13.40 14.56

Fe2O3T 0.79 0.37 1.21 1.23 1.17

TiO2 0.03 0.02 0.08 0.02 0.18

MnO 0.06 0.03 0.16 0.39 0.04

CaO 1.68 1.09 1.42 1.39 1.71

MgO 0.16 0.18 0.02 0.15 0.06

K2O 2.91 2.68 2.02 4.17 4.86

Na2O 4.48 3.85 4.11 3.70 3.42

P2O5 0.18 0.17 0.05 0.11 0.17

LOI 0.59 0.30 0.50 0.26 0.65

total 99.70 99.93 99.89 99.99 99.94

Q 37.7 45.47 41.46 34.86 31.39

Co 0.22 2.87 0.55 0.96

Or 17.16 15.82 11.93 24.61 28.69

Ab 37.86 32.56 34.78 31.26 28.93

An 2.93 4.32 6.73 6.17 7.4

Hy 0.45 0.06 0.38 0.14

Mt 0.11 0.03 0.29 1.22

Hm 0.72 0.35 1.02 0.39 1.17

Ru

Il 0.06 0.04 0.16 0.08

Ap 0.4 0.36 0.1 0.24 0.37

Di 0.85

48

Fig. 15. Classification of igneous rocks by the normative Quartz(Q)-

Alkalifeldspar(A)-Plagiocla se(P) diagram (After Streckeisen, 1976)

(1:alkali feldspar granite, 2:alkali feldspar quartz syenite, 3: alkali feldspar

syenite, 4: syeno granite, 5: monzo granite, 6: granodiorite and 7:quartz

monzonite)

◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak

49

Fig. 16. Classification of igneous rocks by normative Or-An-Ab (After Streckeisen,

1976)

(1: trondhjemite, 2: tonalite, 3: granite, 4: granodiorite, 5: quartz monzonite)

◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak

50

Fig. 17. SiO2 VS molar Al2O3/(Na2O+CaO+K2O) ratio.

◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak

51

Fig. 18. ACF diagram (After Hine et al, 1987)

(A; Al2O3+Fe2O3-(Na2O+K2O), C; CaO-3.3*P2O5, F; FeO+MgO+MnO

◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak )

52

Fig. 19. A'KF diagram (A'; Al2O3+Fe2O3-(Na2O+K2O+CaO), K; K2O, F;

FeO+MgO+MnO

◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak )

53

Table 2. ICP-MA data, in Lichenhills and Outback Nunatak (* : Ferrar dolerite)(ppm)

Sample LH1 LH2 LH3 LH4light LH4gray* LH5 LH6 LH7

Li 38.62 27.06 34.46 11.38 73.82 16.89 13.69 31.42

Be 1.52 3.59 4.11 2.13 2.58 4.74 2.82 2.21

Cr 23.72 3.26 2.62 1.24 9.73 1.71 2.44 5.88

Ga 33.23 27.58 25.80 24.38 39.22 24.07 19.88 29.82

Rb 243.13 219.27 171.96 333.01 176.88 326.77 275.31 297.27

Sr 118.14 88.09 85.29 8.17 129.91 6.31 44.83 68.45

Y 5.60 2.79 2.36 14.81 25.39 4.54 1.12 2.30

Zr 152.41 96.75 72.02 29.98 186.55 26.69 28.88 145.19

Nb 12.54 3.01 3.17 24.53 16.11 31.55 14.56 16.70

Sn 2.29 2.54 2.69 5.85 2.83 5.37 1.95 2.16

Cs 7.78 2.88 3.38 2.20 7.12 3.72 2.17 2.54

Ba 424.13 226.10 157.72 10.52 46.49 13.79 126.66 339.67

Hf 5.63 2.67 2.81 2.26 5.44 2.43 1.67 4.89

V 26.16 8.61 10.58 0.92 22.86 10.34 12.65 21.15

Pb 56.43 47.40 39.27 9.72 23.11 10.25 38.50 47.64

Ta 2.05 nd nd 1.85 1.04 17.40 8.36 1.82

U 4.84 3.68 3.17 2.48 5.46 3.26 3.98 5.81

Th 27.64 14.68 11.67 4.59 29.28 8.77 6.94 24.73

54

LH8 LH9* LH10* LH11* LH12* LH13 LH13-2* LH14 LH15

58.35 77.04 73.32 62.49 46.81 12.34 32.71 27.23 14.40

0.87 1.17 1.68 1.19 12.88 2.49 1.73 1.36 1.42

57.06 59.28 39.16 130.47 66.49 2.42 10.19 3.34 1.75

26.87 31.55 28.89 19.96 35.45 23.02 27.42 24.16 17.00

349.81 294.96 256.87 191.93 362.86 147.10 199.91 184.55 206.15

139.83 476.55 442.02 36.93 47.37 184.67 151.23 71.34 70.29

15.03 5.65 4.73 5.97 2.15 1.84 2.75 2.74 4.28

160.89 92.14 76.58 183.26 75.03 85.27 192.57 82.09 92.81

28.49 22.70 21.62 26.98 36.87 10.20 16.79 2.26 2.69

1.32 1.17 1.12 3.10 1.75 1.69 3.02 1.86 2.23

4.47 11.00 10.41 13.25 7.88 2.56 5.42 2.25 2.35

566.15 503.14 370.87 146.85 553.92 307.81 348.85 262.98 188.20

4.25 2.62 2.22 6.01 2.46 3.11 6.29 2.94 2.84

68.87 193.21 159.89 137.78 143.64 10.11 21.79 12.88 1.30

40.43 3.46 6.01 10.80 31.91 34.93 44.12 44.03 nd

0.87 1.27 1.85 7.65 8.34 2.74 2.99 nd 0.18

2.71 1.21 1.41 4.36 2.62 1.53 4.36 1.81 2.38

25.20 2.48 2.67 16.29 20.38 20.17 44.33 8.68 10.87

55

Sample ON1 ON1-2 ON3 ON5 ON7 ON7-2

Li 11.81 13.65 76.46 242.77 67.90 200.13

Be 8.94 23.90 9.11 7.74 6.05 8.99

Cr 1.81 1.63 1.67 0.75 0.61 3.63

Ga 18.07 16.27 24.49 30.66 18.01 24.96

Rb 422.69 452.38 236.76 217.09 391.19 399.65

Sr 11.52 11.57 10.64 8.72 18.26 42.67

Y 0.99 0.23 1.48 1.84 9.17 2.52

Zr 19.34 8.16 6.48 4.54 74.58 93.91

Nb 22.60 33.71 16.04 31.61 5.91 15.43

Sn 23.11 26.20 42.07 32.68 23.00 27.21

Cs 117.76 90.31 21.68 12.16 25.66 33.52

Ba 31.78 21.52 8.42 9.28 17.89 138.69

Hf 1.80 1.02 0.64 0.17 3.82 3.68

V 8.54 8.52 4.11 0.12 0.15 15.93

Pb 13.58 11.81 13.69 14.76 23.29 33.17

Ta 25.02 11.94 3.78 1.38 0.55 6.18

U 2.78 1.11 1.72 9.80 6.07 8.48

Th 0.55 0.31 1.95 1.09 0.83 20.87

56

Fig. 20. Ternary diagram of Rb-Sr-Ba (after Biste, 1978). The arrow represents

the differentiation trend.

(1: Diorite, 2: Granodiorite & Quartz diorite, 3: Anomalous granite, 4: Normal

granite, 5: Strongly differentiated granite)

(◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak )

57

Fig. 21. Y vs Nb tectonic discriminant diagram (ppm)

(◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak )

58

Fig. 22. Yb vs Ta tectonic discriminant diagram (ppm)

(◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak )

59

Fig. 23.. Rb-(Y-Nb) and Rb-(Yb+Ta) discriminant diagrams

(◆: Igneous rocks from Lichenhills, ●: Igneous rocks from Outback Nunatak )

60

61

Fig. 24. Cl chondrite Normalized REE pattern.

(a: Lichen hills granitic pegmatite , b: Outback nunatak granitic pegmatite)

62

Fig. 25. Primitive mantle Normalized spider diagram..

(a: Lichen hills granitic pegmatite , b: Outback nunatak granitic pegmatite)

63

Fig. 26. Tourmaline observed by microscope.(a, c: ON1-1, b, d: ON1-2,1-3)

64

(a, d: ON3-1, b, e: ON3-2, c, f: ON3-3)

65

(a, c: ON5-1, b, d: ON5-2)

66

(a: ON7-1-, b: ON7-3, c: ON7-5, d: ON7-2, e: ON7-4, f: ON7-6)

67

Fig. 27. BSE image of Tourmaline(a:ON1-1, b: ON 1-2, c: ON 1-3, d: ON 3-1, e: ON 3-2, f: ON 3-3, g: ON 5, h: ON 7-1, i:

ON7-2, j: ON7-3, k: ON7-4, l: ON7-5, m: ON7-6)

68

69

70

71

72

73

74

Fig. 28. Common tourmaline end member and Triangular diagram showing

(Henry and Guidotti, 1985)

75

Table 3. Microprobe analyses of colored zones of tourmalines from Outback

Nunatak

core rim core rim core rim

SiO2 36.07 35.89 36.45 36.45 35.51 34.73

TiO2 0.08 0.41 0.08 0.08 0.04 0.36

Al2O3 34.34 34.61 35.81 35.81 34.59 35.32

FeO 14.35 13.62 13.59 13.59 13.59 12.49

MnO 0.28 0.27 0.25 0.25 0.24 0.18

MgO 0.72 1.19 0.68 0.68 0.70 1.41

CaO 0.07 0.15 0.06 0.06 0.07 0.15

Na2O 1.54 1.77 1.50 1.50 1.49 1.71

K2O 0.04 0.03 0.03 0.03 0.03 0.03

ZnO 0.12 0.16 0.10 0.10 0.08 0.21

Total 87.59 88.10 88.55 88.55 86.34 86.58

ON 1-1 ON 1-2 ON 1-3

core rim core rim core rim

Si 5.9726 5.9022 5.9321 5.9321 5.9403 5.7832

Al 6.7034 6.7086 6.8694 6.8694 6.8212 6.9319

Al in Y 0.6891 0.6787 0.8150 0.8150 0.7686 0.7743

Ti 0.0098 0.0511 0.0102 0.0102 0.0053 0.0446

Ca 0.0115 0.0259 0.0110 0.0110 0.0127 0.0275

Na 0.4955 0.5634 0.4740 0.4740 0.4830 0.5534

Na/(Na+Ca) 0.9773 0.9560 0.9773 0.9773 0.9743 0.9527

K 0.0082 0.0069 0.0060 0.0060 0.0064 0.0064

Fe 1.9874 1.8733 1.8503 1.8503 1.9009 1.7388

Mg 0.1768 0.2905 0.1645 0.1645 0.1741 0.3500

Fe/(Fe+Mg) 0.9183 0.8658 0.9184 0.9184 0.9161 0.8324

Mn 0.0386 0.0370 0.0342 0.0342 0.0343 0.0255

X-site 0.5153 0.5962 0.4910 0.4910 0.5021 0.5873

Y-site 2.2027 2.2008 2.0490 2.0490 2.1093 2.1144

Z-site 6.7165 6.7765 6.8829 6.8829 6.8282 6.9911

X=Na+Ca+K

Y=Fe+Mg+Mn

Z=Al+1.33Ti

Cations on the basis of 24.5 oxygens

76

core rim core rim core rim

SiO2 35.54 34.65 34.26 34.70 39.18 36.36

TiO2 0.85 0.93 0.28 0.86 0.30 0.97

Al2O3 34.62 35.09 35.13 35.13 38.32 35.78

FeO 11.71 11.66 11.71 11.49 12.72 12.87

MnO 0.17 0.12 0.14 0.15 0.19 0.13

MgO 2.58 2.98 2.29 2.87 2.22 3.00

CaO 0.28 0.38 0.13 0.34 0.16 0.34

Na2O 1.80 2.01 1.55 1.86 1.65 1.99

K2O 0.04 0.05 0.03 0.03 0.03 0.04

ZnO 0.14 0.12 0.18 0.13 0.10 0.14

Total 87.74 87.99 85.69 87.56 94.87 91.60

core rim core rim core rim

Si 5.8242 5.6780 5.7426 5.7014 5.9059 5.7405

Al 6.6870 6.7782 6.9411 6.8047 6.8095 6.6579

Al in Y 0.6505 0.6087 0.7304 0.6473 0.7602 0.5509

Ti 0.1048 0.1146 0.0350 0.1062 0.0337 0.1147

Ca 0.0488 0.0662 0.0234 0.0593 0.0254 0.0568

Na 0.5732 0.6380 0.5029 0.5929 0.4817 0.6085

Na/(Na+Ca) 0.9215 0.9060 0.9556 0.9090 0.9500 0.9146

K 0.0082 0.0094 0.0062 0.0061 0.0063 0.0083

Fe 1.6051 1.5977 1.6423 1.5790 1.6041 1.6985

Mg 0.6305 0.7284 0.5710 0.7032 0.4984 0.7062

Fe/(Fe+Mg) 0.7180 0.6868 0.7420 0.6919 0.7629 0.7063

Mn 0.0240 0.0171 0.0200 0.0210 0.0236 0.0167

X-site 0.6302 0.7136 0.5324 0.6583 0.5134 0.6736

Y-site 2.2596 2.3432 2.2334 2.3032 2.1262 2.4215

Z-site 6.8264 6.9306 6.9878 6.9459 6.8543 6.8104

X=Na+Ca+K

Y=Fe+Mg+Mn

Z=Al+1.33Ti

ON 3-1 ON 3-2 ON 3-3

Cations on the basis of 24.5 oxygens

77

core mid 1 mid 2 rim core rim

SiO2 35.693 36.262 35.99 37.141 36.918 35.67

TiO2 0.254 0.42 0.261 0.734 0.232 0.806

Al2O3 35.363 36.293 35.542 35.027 35.17 34.028

FeO 12.488 12.325 12.331 12.391 12.531 12.284

MnO 0.126 0.125 0.151 0.149 0.122 0.154

MgO 1.71 1.892 1.746 2.102 1.705 2.353

CaO 0.103 0.136 0.124 0.248 0.119 0.263

Na2O 1.481 1.616 1.477 1.791 1.519 1.793

K2O 0.027 0.036 0.031 0.035 0.035 0.04

ZnO 0.143 0.109 0.102 0.165 0.17 0.17

Total 87.388 89.215 87.754 89.782 88.521 87.56

core mid 1 mid 2 rim core rim

Si 5.8667 5.8306 5.8817 5.9442 5.9806 5.8732

Al 6.8511 6.8784 6.8465 6.6076 6.7155 6.6041

Al in Y 0.7595 0.7765 0.7708 0.6693 0.7336 0.6100

Ti 0.0314 0.0508 0.0321 0.0883 0.0283 0.0998

Ca 0.0181 0.0234 0.0217 0.0425 0.0207 0.0464

Na 0.4720 0.5038 0.4680 0.5558 0.4771 0.5724

Na/(Na+Ca) 0.9630 0.9556 0.9557 0.9289 0.9585 0.9250

K 0.0057 0.0074 0.0065 0.0071 0.0072 0.0084

Fe 1.7166 1.6574 1.6854 1.6585 1.6977 1.6916

Mg 0.4190 0.4535 0.4254 0.5015 0.4117 0.5775

Fe/(Fe+Mg) 0.8038 0.7852 0.7985 0.7678 0.8048 0.7455

Mn 0.0175 0.0170 0.0209 0.0202 0.0167 0.0215

X-site 0.4958 0.5346 0.4962 0.6055 0.5050 0.6272

Y-site 2.1531 2.1279 2.1316 2.1802 2.1262 2.2906

Z-site 6.8928 6.9459 6.8891 6.7251 6.7531 6.7368

X=Na+Ca+K

Y=Fe+Mg+Mn

Z=Al+1.33Ti

ON 5-1 ON 5-2

Cations on the basis of 24.5 oxygens

78

core mid rim core rim core rim core mid rim core mid rim core rim

SiO2 37.12 36.06 35.31 35.61 35.44 36.52 35.45 37.29 35.64 37.13 35.98 35.99 35.32 37.06 36.10

TiO2 0.21 0.70 0.73 0.20 0.64 0.21 0.60 0.20 0.73 0.79 0.22 0.74 0.49 0.18 0.12

Al2O3 34.83 34.17 34.26 36.18 36.49 35.95 35.22 35.12 35.28 34.53 34.94 34.58 34.29 34.67 35.12

FeO 10.88 12.38 13.55 13.34 13.97 11.33 13.86 10.79 13.71 11.51 12.44 11.65 13.73 11.23 13.35

MnO 0.13 0.25 0.39 0.40 0.60 0.15 0.58 0.13 0.42 0.13 0.28 0.15 0.66 0.23 0.26

MgO 2.66 1.88 0.80 0.55 0.45 2.36 0.42 2.75 0.73 3.15 1.43 3.07 0.32 2.18 1.05

CaO 0.12 0.20 0.15 0.06 0.13 0.11 0.16 0.10 0.18 0.32 0.08 0.30 0.13 0.10 0.08

Na2O 1.54 1.77 1.67 1.39 1.71 1.53 1.65 1.57 1.71 1.93 1.46 1.97 1.65 1.49 1.58

K2O 0.03 0.04 0.04 0.02 0.04 0.02 0.04 0.02 0.04 0.04 0.03 0.04 0.05 0.02 0.03

ZnO 0.12 0.16 0.18 0.24 0.28 0.21 0.27 0.08 0.21 0.15 0.20 0.17 0.23 0.13 0.29

Total 87.64 87.61 87.08 88.01 89.75 88.38 88.24 88.07 88.64 89.69 87.04 88.72 86.86 87.29 87.97

ON 7-1 ON 7-2 ON 7-3 ON 7-4 ON 7-5 ON 7-6

79

core mid rim core rim core rim core mid rim core mid rim core rim

Si 6.0205 5.9284 5.8816 5.8389 5.7409 5.8943 5.8377 6.0144 5.8339 5.9355 5.9365 5.8371 5.9089 6.0462 5.9254

Al 6.6599 6.6218 6.7260 6.9928 6.9672 6.8395 6.8372 6.6760 6.8060 6.5056 6.7954 6.6119 6.7611 6.6664 6.7945

Al in Y 0.7140 0.6649 0.7297 0.8644 0.8125 0.7673 0.7738 0.7230 0.7595 0.5667 0.7673 0.5690 0.7527 0.7420 0.7401

Ti 0.0253 0.0863 0.0918 0.0245 0.0785 0.0251 0.0743 0.0245 0.0899 0.0944 0.0267 0.0903 0.0621 0.0221 0.0152

Ca 0.0216 0.0351 0.0273 0.0107 0.0229 0.0197 0.0282 0.0180 0.0309 0.0550 0.0138 0.0516 0.0233 0.0170 0.0142

Na 0.4847 0.5636 0.5388 0.4426 0.5380 0.4782 0.5282 0.4894 0.5427 0.5976 0.4658 0.6193 0.5352 0.4707 0.5013

Na/(Na+Ca) 0.9574 0.9414 0.9518 0.9764 0.9592 0.9604 0.9493 0.9646 0.9462 0.9157 0.9712 0.9231 0.9583 0.9652 0.9724

K 0.0052 0.0073 0.0085 0.0050 0.0079 0.0031 0.0074 0.0049 0.0084 0.0071 0.0057 0.0081 0.0102 0.0050 0.0052

Fe 1.4755 1.7024 1.8877 1.8297 1.8920 1.5286 1.9089 1.4552 1.8766 1.5386 1.7170 1.5798 1.9205 1.5321 1.8327

Mg 0.6441 0.4605 0.1989 0.1347 0.1075 0.5683 0.1019 0.6599 0.1771 0.7508 0.3510 0.7414 0.0793 0.5294 0.2569

Fe/(Fe+Mg) 0.6961 0.7871 0.9047 0.9314 0.9463 0.7290 0.9493 0.6880 0.9137 0.6720 0.8303 0.6806 0.9603 0.7432 0.8771

Mn 0.0181 0.0350 0.0550 0.0558 0.0819 0.0201 0.0809 0.0183 0.0588 0.0181 0.0391 0.0212 0.0928 0.0316 0.0356

X-site 0.5114 0.6060 0.5746 0.4583 0.5688 0.5010 0.5638 0.5123 0.5820 0.6597 0.4853 0.6790 0.5687 0.4926 0.5207

Y-site 2.1378 2.1978 2.1416 2.0202 2.0814 2.1170 2.0917 2.1334 2.1125 2.3075 2.1071 2.3423 2.0926 2.0932 2.1252

Z-site 6.6935 6.7365 6.8482 7.0255 7.0716 6.8730 6.9361 6.7085 6.9255 6.6311 6.8309 6.7320 6.8438 6.6957 6.8147

Cations on the basis of 24.5 oxygens

80

Fig. 29. Al-Fe(tot)-Mg diagram ( in molecular proportions) for tourmalines from

Outback Nunatak rocks. (After Henry and Guidotti, 1985 and Plimer and Lees,

1988). (1) Li -rich granitoid pegmatites and aplites, (2) Li-poor granitoids and

their associated pegmatites and aplites, (3) Fe3+-rich quartz-tourmaline rocks

(hydrothermally altered agrnites, (4) Metapelites and metapsammites co-exiting

with an Al-saturating phase, (5)Metapelites and metapsammites not coexisting

with an Al-saturating phase, (6) Fe3+-rich quartz-tourmaline rocks, calc silicate

rocks and metapelites, (7) Low-Ca metaultramafics and Cr, V-rich metasediments,

(8) Metacarbonates and metapyroxenites, (9) Ca-rich metapelites and (10) Ca-

poor metapelites, metapsammites and quartz-tourmaline rocks.

black circle: core of tourmalines, red circle: rim of tourmalines.

81

Fig. 30. Ca-Fe(tot)-Mg diagram (in molecular proportions) for tourmalines from

Outback Nunatak rocks. (After Henry and Guidotti, 1985 and Plimer and Lees,

1988). (1) Li -rich granitoid pegmatites and aplites, (2) Li-poor granitoids and

their associated pegmatites and aplites, (3) Ca-rich metapelites, metapsammites,

and calc-silicate rocks, (4) Ca-poor metapelites, metapsammites, and quartz-

tourmaline rocks, (5) Metacarbonates and (6) Metaultramafics.

black circle: core of tourmalines, red circle: rim of tourmaline.

82

Fig. 31. Compositional variation in four tourmaline grains from Outback Nunatak.

83

Fig. 32. Plots of cation occupancies of tourmaline from Outback

Nunatak. Fe/Mg ratio; schorl-dravite plot along the line

∑(Fe+Mg)=3 ; values of ∑(Fe+Mg) < 3 correspond to Al

substitiution in Y ; values of ∑(Fe+Mg) >3 would plot in the

ferrischorl region.

84

Fig. 33. Plots of cation occupancies of tourmaline from Outback

Nunatak. The sum of sites X+Y vs. Z.

Fig. 34. Plots of cation occupancies of tourmaline from Outback

Nunatak. Variations of Fe/(Fe+Mg) vs. Al in Y.

85

86

국문 초록

남극 북빅토리아 랜드, 라이켄 힐즈,

아웃백 누나탁 지역의 화강암질

페그마타이트의 광물학적 지구화학적 연구

페그마타이트는 화강암과 유사한 조성을 가진 거정질 암석이다.

이러한 페그마타이트에는 붕소 함유량이 높은 전기석이 다량

함유되어 있다. 전기석의 일반적인 화학식은

XY3Z6Si6B3O27(OH,O,F)4와 같다. 이러한 전기석은 퇴적 및 암석

형성 당시 환경에 대한 정보를 제공해준다. 그렇기 때문에

암석발생학적 지시자로서 증요성을 가지고 있다. 또한, 결정 내 화학

조성의 변화는 전기석 결정 생성 당시의 물리적, 화학적 변화를

내포한다. 이번 연구 지역은 남극 북빅토리아 랜드 내 위치한

라이켄힐즈, 아웃백누나탁 지역이다. 라이켄힐즈 지역의 암상은

화강암질 암석과, 우백질 화강암, 조립현무암으로 구성되어 있다.

아웃백누나탁 지역의 경우에는 화강암질 페그마타이트와 선캠브리아

편암으로 구성된다. 두 지역의 암상은 같은 Granite Hobour

Intrusive 이지만 세부적 기원에 있어 차이점을 보인다. 라이켄힐즈

87

지역의 암석의 경우 좀 더 S-type에 가까운 모습을 보인다. 또한,

아웃백누나탁 페그마타이트에서는 전기석이 잘 관찰된다. 거정질의

전기석에는 001면으로 화학적 누대구조가 잘 발달되어 있다. 이러한

전기석은 화학 분석시 스코올-엘바이트 고용체에 속하며 Li, Mg

양이 부족하고 Al, Fe가 풍부한 환경에서 형성되었음을 지시한다.

중심에서 가장자리로 갈수록 페리스코올 치환이 일어나게 되는데

이는 전기석의 가장자리 형성 시기에 열수의 유입으로 인한 산화

상태의 증가나 높은 산화 상태를 가진 지상수의 혼합 혹은 열수의

끓음을 암시한다.

주요어 : 페그마타이트, 전기석, 암석발생학적 지시자 , S-type 화강암,

화학적 누대구조 , 스코올, 엘바이트, 페리스코올 치환

Student Number : 2014 - 20326

1. Introduction 2. Geological Setting & Sample information 3. Method 4. Result and Discussion 4.1 Macroscopy & Microscope observation 4.2 Chemical composition 4.3 Tourmaline observation 4.4 Tourmaline geochemistry

5. Conclusion 6. Reference Figures, Tables Abstract in Korean

121. Introduction 12. Geological Setting & Sample information 33. Method 64. Result and Discussion 9 4.1 Macroscopy & Microscope observation 9 4.2 Chemical composition 12 4.3 Tourmaline observation 17 4.4 Tourmaline geochemistry 195. Conclusion 246. Reference 27Figures, Tables 31Abstract in Korean 86