exhumation of ultrahigh-pressure metamorphic oceanic crust

Exhumation of ultrahigh-pressure metamorphicoceanic crust from Lago di Cignana,

Piemontese zone, Western Alps

Dissertation

zur Erlangung des Grades eines

Doktors der Naturwissenschaften der

Fakultät für Geowissenschaften an

der Ruhr-Universität Bochum

vorgelegt von

Sebastiaan Nicolaas Gerardus Cornelis van der Klauw

aus Gouda (Niederlande)

Bochum 1998

Als Dissertation genehmigt von der Fakultät für

Geowissenschhaften der Ruhr-Universität Bochum

Tag der Disputation: 11. Mai 1999

Promotionskomission:

Vorsitzender: Prof. Dr. Dr. h.c. L. Dresen

Erster Gutachter: Prof. Dr. B. Stöckhert

Zweiter Gutachter: Prof. Dr. W. Schreyer

Fachfremder Gutachter: Prof. Dr. B. Marschner

iii

Kurzfassung

Zur Entschlüsselung der Exhumierungsgeschichte ehemaliger ozeanischer Kruste im Gebiet

des Lago di Cignana, Valtournanche, in den Westalpen wurden die hier vorkommenden ultrahoch-

druckmetamorphen Coesit-führenden Basalte und Sedimentgesteine untersucht. Unter Einbeziehung

von Altersbestimmungen aus der Literatur werden mögliche Exhumierungsprozesse eingegrenzt.

In den metabasischen Gesteinen ist folgende Geschichte aufgezeichnet: Unter ultrahochdruck-

metamorphen Bedingungen (ca. 600 °C, 2,7 GPa) wurden die Eklogite durch Versetzungskriechen

von Omphacit verformt. Scherbänder belegen eine Lokalisierung der Verformung. Für die ersten

50 km der Exhumierung existieren keine Aufzeichnungen, was suggeriert, dass die Verformung

außerhalb des Aufschlussbereiches lokalisiert war. Bei Druck- und Temperaturbedingungen von

1,2 GPa und 500 °C wurde ein kleiner Teil der ultrahochdruckmetamorphen Minerale statisch

ersetzt. Weitere statische Ersetzungen benötigte Fluid-Infiltration entlang von Zugrissen, die jetzt

als Quarzgänge vorliegen. Form und Orientierung der verschiedenen Generationen von Quarzgängen

deuten auf niedrige Differentialspannungen hin. Die Ganggenerationen können mit den Stadien

des Ersatzes der ultrahochdruckmetamorphen Minerale korreliert werden. So kann eine Änderung

in der Orientierung des Spannungsfeldes und eine Zunahme der Differentialspannung bei Tempera-

turen um 500 °C und Drücken um 0,8 GPa abgeleitet werden.

Bei Druck- und Temperaturbedingungen von unter 0,6 GPa und 450 °C wurden die meta-

sedimentären Gesteine durchgreifend verformt, wobei sämtliche früher angelegten Strukturen über-

prägt wurden. In den Eklogiten fand die Verformung lokal statt und führte zur Bildung von

Grünschiefern. Mikrostrukturen in den Quarzgängen belegen für dieses Ereigniss eine Verformung

durch Versetzungskriechen von Quarz. Weitere Verformung war lokalisiert und fand bei Tempera-

turen um 350 °C und höheren Differentialspannungen statt. Die Dichte von Fluideinschlüssen belegt

eine Abkühlung unter 300 °C bei Drücken zwischen 0,2 und 0,4 GPa. Eine spätere spröde Ver-

formung konnte mit dem Druck-Temperatur-Pfad nicht in Bezug gesetzt werden.

Der Vergleich von publizierten radiometrischen Altersbestimmungen mit der Entwicklungsge-

schichte zeigt, dass die Exhumierung in zwei Phasen ablief. Die Exhumierung aus einer Tiefe von

etwa 90 km bis auf etwa 25 km fand innerhalb weniger Millionen Jahre bei niedrigen Differential-

spannungen statt. Das Model eines Subduktionskanals mit einer Zone entgegengesetzt gerichteten

Flusses passt zu dieser Entwicklungsgeschichte. Die Exhumierung von etwa 25 km bis auf etwa 10

km Tiefe fand langsamer und bei höheren Differentialspannungen statt. Dieser Teil der Entwicklungs-

geschichte wird im Einklang mit Konzepten zur regionalen Geologie wie folgt interpretiert. Auf

eine Stapelung von Decken folgte die Exhumierung durch Extension der verdickten Kruste an

flach einfallenden Abschiebungen.

iv

Abstract

The metamorphic and structural history of coesite-bearing ultra high pressure metamorphic oceanic

crust at Lago di Cignana, Valtournanche, Western Alps, recorded during exhumation has been

resolved. The record of metamorphic oceanic crust consisting of metabasalts and metasedimentary

rocks combined with geochronologic data from the literature is used to constrain possible exhumation

mechanisms.

In the metabasic rocks following history has been recorded: At ultra high pressure metamorphic

conditions (ca. 600 °C, 2.7. GPa) the eclogites were deformed by dislocation creep of omphacite.

The deformation was progressively localised into shearbands. A gap in the record for the first

50 km of subsequent exhumation suggests that any deformation during this time was localised

outside the outcrop area. At pressure and temperature conditions of 1.2 GPa and 550 °C the record

shows static replacement of a minor part of the ultra high pressure metamorphic mineral assemblage

in small scale closed systems. Further static replacement required fluid infiltration, concentrated

along tensile fractures now represented by veins. Shape and orientation of the several vein generations

indicate relatively low differential stresses. The vein generations can be correlated with replacement

stages of the ultra high pressure metamorphic minerals. In this way, a change in the orientation of

the stress field and an increase of the differential stress can be inferred at a temperature of around

500 °C and a pressure of 0.8 GPa.

At pressure and temperature conditions below 0.6 GPa and 450 °C intense deformation wiped

out all structures that might have formed earlier in the metasedimentary rocks. Localised ductile

deformation transformed part of the eclogites to greenschists. Microstructures of quartz veins

deformed during this stage indicate deformation by dislocation creep of quartz. This was followed

by a period of low differential stress. Localised deformation occurred at temperatures of ca. 350 °C

and at higher differential stresses. The densities of fluid inclusion suggest cooling to below ca.

300 C° at pressures between 0.2 and 0.4 GPa. Later deformation that occurred in the brittle field

could not be correlated with the pressure and temperature path.

The combination of this pressure-temperature-deformation-record with published geochronologic

data indicates a two stage exhumation. Exhumation from depths of approx. 90 km to depths of

approx. 25 km took place in at maximum a few million years and with low differential stresses in

the rock. For this exhumation stage the concept of a subduction channel with a zone of reverse flow

remains within the constraints posed by the record. Exhumation from depths of approx. 25 km to

approx. 10 km was slower and differential stresses were higher. This part of the record is in

conjunction with the regional geologic framework interpreted to represent the stacking of thrust

slices, followed by extension along low angle normal faults to explain exhumation.

v

Acknowledgments

This study became possible due to financial support from the German Science Foundation as

part of the Research group „High-pressure metamorphism in nature and experiment“ at the Ruhr-

University Bochum. This study was initiated by Prof. Dr. Bernard Stöckhert and Dr. Thomas

Reinecke, who both through numerous discussions and critical comments focused my thinking

about exhumation of high pressure metamorphic rocks. I must also thank numerous other persons

at the Institute of Geology and the Institute of Mineralogy and will risk to forget more than a few by

mentioning some.

I will start with Mr Gilsing and Mr Eickhoff, who prepared, usually in remarkably short time, a

large number of thin sections for me. Next on the list are Dr. Bernhardt and Mr Köhler-Schnettger

who kept the electron microprobe in running order. For SEM and CL photographs I have to thank

Dr. Rolf Neuser and Dirk Habermann. Dirk and Peter Wagner-Zweigel are also thanked for the

good time we had in the Alps. Thanks are also due for Mr Reß and Mrs Aschenbrenner for numerous

quickly delivered photographs.

The many computerprograms written by Klaus Röller made data interpretation much easier. I

should not forget to thank all the colleagues who introduced me to different analytical methods.

I like to thank my former roommates at the institute Petra Heckhoff, Sybille Schwarz and Andreas

Toetz for their introduction to the Ruhr-University. Finally, all colleagues from Bochum and Jena,

who spent time for discussions with beer, coffee, etc., are also thanked.

vi

Contents

Kurzfassung iii

Abstract iv

Acknowledgments v

Contents vi

List of abbreviations ix

List of tables xii

List of photographs xv

List of figures xvi

1 Introduction 1

2 Regional Geology 2

2.1 The studied Area 5

3 The record in the metabasic rocks 6

3.1 Petrology of the metabasic rocks - eclogites and greenschists 6

3.1.1 Group 0 eclogites 8

3.1.1.1 Mineral compositions 8

3.1.1.2 Mineral paragenesis and PT-estimates 13






3.1.3.2 Mineral paragenesis and PT- estimates 23




3.1.5 Group 4 eclogites and greenschists 26



3.2 Structures in the eclogites 27

3.3 Structures in the greenschists 33

vii

4 The record in the metasedimentary rocks 34

4.1 Petrology of the metasedimentary rocks 34

4.2 Structures in the metasedimentary rocks 34

5 Quartz veins (microstructures, fabrics and fluid inclusions) 38

5.1 Microstructures of vein quartz 38

5.2 Paleopiezometry 39

5.3 C-axis fabrics in quartz veins 41

5.3.1 Eclogites 41

5.3.2 Metasedimentary rocks 43

5.3.3 Summary 44

5.4 Fluid inclusions in vein quartz 44

5.4.1 Compositions and densities of the fluid inclusions. 47

6 The exhumation record of the rocks 50

6.1 The record during UHPM and early exhumation 50

6.2 The record between 575 and ca. 450 °C 52

6.3 The record between ca. 450 and 300 °C 54

6.4 Synthesis: A two stage exhumation for the UHPM rocks of Lago di Cignana 55

7 Discussion and Exhumation concepts 58

7.1 Exhumation theories 58

7.1.1 Exhumation through erosion 58

7.1.2 Exhumation by extension tectonics 59

7.1.2.1 The critical wedge concept 60

7.1.2.2 The lithospheric extension concept 61

7.1.2.3 The subduction zone roll back concept 62

7.1.2.4 Concepts that require a period of divergence 62

7.1.3 Upflow concepts 63

7.2 Evaluation of published exhumation scenarios for exhumation from depths of 65

approx. 90 km to 25 km

7.3 Scenario for exhumation from 90 to 25 km depth 66

7.4 The scenario for the later exhumation from depths of ca. 25 km to the surface 69

8 Conclusions 72

9 References 74

Curriculum vitae

viii

Appendix A Methods A-1

A1 Sampling A-1

A2 Preparation A-1

A3 Analytical methods A-2

Appendix B Geothermobarometry B-1

B1 Thermometers B-1

B1.1 Garnet clinopyroxene thermometry B-1

B1.2 Amphibole Plagioclase thermometry. B-3

B1.3 Calcite - Dolomite thermometry B-4

B2 Barometers B-4

Tables with calculated temperatures and pressures B-6

Appendix C Tables C-1

C1 Sample list C-1

C2 Whole rock analyses C-5

C3 Tables of mineral compositions C-6

ix

List of abbreviations

° degree

°C degree Celsius

α angle between surface of the orogenic wedge and the horizontal

β angle between the basal decollement of the orogenic wedge and the horizontal

∆-velocity difference between the velocity of the downgoing plate and the material in the subduction channel close

to the plate-channel interface

θ frontal angle of the orogenic wedge

µ shear modulus

µm micrometer, 10-6m

µm2 square micrometer

ρ density

σ sigma, standard deviation

σ1

largest principal stress

σ3

smallest principal stress

τb

shear stress along the basal decollement of the orogenic wedge

A&E87 Anovitz & Essene, 1987

A94 Ai, 1994

ab albite

acm acmite, or acmite component in clinopyroxene

adr andradite, or andradite component in garnet

ae aegerine, or aegerine component in clinopyroxene

aggr. aggregate

alm almandine, or almandine component in garnet

amp gln rims of blue-green amphibole around glaucophane

amp grt discontineous overgrowth of blue-green amphibole on garnet

amp amphibole

an anorthite, or anorthite component in plagioclase

ap apatite

app appendix

approx. approximately

arg aragonite

b burgers vector

B88 Berman, 1988

biot green brown mica

BSE back scattered electron

c core position

ca. circa

cal calcite

cf. confer

chl chlorite

CL cathodoluminescence

cm centimeter

cm3 cubic centimeter

cpx clinopyroxene

cs coesite

czo clinozoisite

x

D deformation

d grain size

D1e

first deformation stage in eclogites

D2g

second deformation stage in the greenschists

D2s

second deformation stage in the metasedimentary rocks

D3e

third deformation stage in the eclogites

D3g

third deformation stage in the greenschists

D3s

third deformation stage in the metasedimentary rocks

D4e

fourth deformation stage in the eclogites

D4e1

number one shearzone of the fourth deformation stage in the eclogites

D4e2

number two shearzone of the fourth deformation stage in the eclogites

D4g

fourth deformation stage in the greenschists

D4s

fourth deformation stage in the metasedimentary rocks

D5g

fifth deformation stage in the greenschists

D5s

fifth deformation stage in the metasedimentary rocks

DEDM Digital Element Distribution Map

diop diopide, or diopside component in clinopyroxene

dol dolomite

Dr. Doctor

E east

ein eclogite

E&G79 Ellis & Green, 1979

e.c.c. extensional crenulation cleavage

e.g. example given

ENE east-north-east

eq. equivalent

exhum. exhumation

Fig. figure

g gravity

gln glaucophane

GPa giga Pascal (109 Pascal, 10 kilobar)

gr gramm

grs grossular, or grossular component in garnet

grt garnet

h thickness of the orogenic wedge

H&B94 Holland & Blundy, 1994

H79 Holland, 1979

hed hedenbergite, or hedenbergite component in clinopyroxene

HP high pressure

HPM high pressure metamorphic

ilm ilmenite

J&P71 Johannes & Puhan, 1971

jd jadeite, or jadeite component in clinopyroxene

K Kelvin

K88 Krogh, 1988

km kilometer

Kn

constant in the recrystallised grain size paleopiezometer

kV kilovolt

xi

L1e

stretching lineation of the first deformation stage in eclogites

L2s

stretching lineation of the second deformation stage in the metasedimentary rocks

l-ab low albite

m meter

m.y. million years

m2 square meter

Ma million years before present

max. maximum

mc microcline

min. minimum

mm millimeter, 10-3 m

MORB mid ocean ridge basalt

MPa mega Pascal, (106 Pascal, 0,1 kbar)

n constant in the recrystallised grain size paleopiezometer

N north

NE north-east

NNE north-north-east

NNW north-north-west

NW north-west

omp omphacite, or omphacite component in clinopyroxene

P pressure

P&N89 Pattison & Newton, 1989

P85 Powell, 1985

Pa Pascal

Pf

pore fluid pressure

pfu per formula unit

pg paragonite

phe phengite

pl plagioclase

prp pyrope, or pyrope component in garnet

PT pressure and temperature

qtz quartz

quad quadrilateral pyroxene

r rim position

rt rutile

sin metasedimentary rock

s second

S south

s-1 per second

S1e

foliation of the first deformation stage in eclogites

S1g

foliation of the first deformation stage in the greenschists

S2e

foliation of the second deformation stage in eclogites

S2g

foliation of the second deformation stage in the greenschists

S2s

foliation of the second deformation stage in the metasedimentary rocks

S3e

foliation of the third deformation stage in the eclogites

S3s

foliation of the third deformation stage in the metasedimentary rocks

SE south-east

SEM scanning electron microscope

xii

sps spessartine, or spessartine component in garnet

SSW south-south-west

SW south-west

sympl symplectite

T temperature

t time

Te tensile strength

Teut

eutectic temperature

Thom

homogenisation temperature

tlc talc

Tm

melting temperature

tot total

ttn titanite

UHP ultra high pressure

UHPM ultra high pressure metamorphic

V volume

vol.% volume percent

W west

WNW west-north-west

WSW west-south-west

wt.% weight percent

X maximum principal strain axis

Y intermediate principal strain axis

Z minimal principal strain axis

zoi zoisite

Z-S Zermatt Saas

List of Tables

Table 1 2

Pressure and temperature estimates of different authors for the high pressure metamorphism and later reequilibration

of rocks from the Zermatt Saas zone.

Table 2 7

The UHPM mineral assemblage and the lower PT-replacement products formed at their expense in the different

eclogite groups.

Table 3 14

Temperatures (at 2.7. GPa) calculated with different calibrations of the grt-cpx thermometer for some representative

grt and omp combinations.

Table 4 20

Pressures (at 550 °C) calculated with the jad(in omp)+qtz=ab barometer of Holland (1980).

Table 5 22

Temperatures calculated with the calcite-dolomite thermometer of Anovitz & Essene (1987) for some representative

cal analyses in domains with different cl colours.

xiii

Table 6 27

Mineral compositions of the minerals used by Evans (1990) to construct his petrogenetic grid and the composition

of these minerals in the metabasic rocks at Lago di Cignana.

Table 7 48

Temperature ranges for observed phase transformations and inferred composition and densities of early and late

fluid inclusions from the investigated samples.

Table 8 53

Correlation between the degree of lower PT-replacement and the number of veins present in a rock volume.

Appendix B

Table B1 B-2

Parameters for the Pattison & Newton (1989) calibration of the garnet clinopyroxene thermometer

Table B2 B-6

Temperatures calculated with different calibrations of the garnet clinopyroxene thermometer for several garnet

clinopyroxene pairs

Table B3 B-7

Temperatures for the growth of albite-amphibole-symplectites calculated with the amphibole-plagioclase

thermometer (Holland & Blundy, 1994).

Table B4 B-4

Regression parameters for the Anovitz & Essenne (1987) calibration of the calcite dolomite solvus thermometer in

the system CaCO3 - MgCO

3 and the system CaCO

3 - MgCO

3-FeCO

3 .

Table B5 B-12

Temperatures for the onset of dolomite decomposition calculated with the calcite-dolomite solvus thermometer

(Anovitz & Essenne, 1987).

Table B6 B-14

Pressures for the onset of omphacite decomposition calculated with the jadeite quartz and albite barometer (Holland,

1980) at a temperature of 550 °C.

Appendix C

Table C1 C-1

list of samples

Table C2 C-5

Whole rock analyses for major and trace elements from samples of group 1 to 4 eclogites.

Table C3 C-6

omphacite compositions

Table C4 C-15

garnet compositions

xiv

Table C5 C-26

glaucophane compositions

Table C6 C-28

clinozoisite compositions

Table C7 C-33

zoisite compositions

Table C8 C-34

paragonite compositions

Table C9 C-37

phengite compositions

Table C10 C-40

rutile compositions

Table C11 C-41

dolomite compositions

Table C12 C-41

calcite compositions

Table C13 C-43

albite compositions

Table C14 C-45

compositions of amphibole around garnet

Table C15 C-47

compositions of amphibole around glaucophane

Table C16 C-48

compositions of amphibole in symplectite

Table C17 C-51

titanite compositions

Table C18 C-53

ilmenite compositions

Table C19 C-53

compositions of dark mica between garnet and phengite

Table C20 C-54

coarse grained green amphibole compositions

Table C21 C-55

chlorite compositions

Table C22 C-59

epidote compositions

xv

List of Photographs

Photo 1 12

Typical coesite inclusion in omphacite with a small rim of quartz between omphacite and coesite. Plane polarised

light, length of photograph 1.4 mm.

Photo 2 12

Coesite inclusion in omphacite, with a small rim of quartz between cs and omp. Plane polarised light, length of

photograph 1.4 mm.

Photo 3 15

A digital element distribution map for Mn in grt. Length of the picture ca. 5 mm.

Photo 4 16

Gln rimmed by blue-green amp (amp gln) in a matrix of omp. Plane polarised light, long side of the photograph is

1.4 mm.

Photo 5 16

B(ack)S(cattered)E(lectron) photograph of the rim of blue- green amp around gln.

Photo 6 19

Cathodoluminescence photograph of cal in a dolomite domain. Long side of the photograph is 3.8 mm.

Photo 7 19

Late replacement of grt by chl and epidote (czoV). Crossed polars, long side of the photograph is 7 mm.

Photo 8 36

A lens of high viscous eclogite in a matrix of low viscous metasedimentary rocks. The assymmetric structure

suggests a high degree of non coaxial deformation. N is up, length of eclogitic lens is ca. 0.5 m.

Photo 9 36

Dust trails in vein albite, define an older growth structure. Crossed polars, long side of photograph is 7 mm.

Photo 10 38

Microstructure of a type IIe quartz vein close to a late shearzone. Crossed polars, long side of the photograph is

7 mm.

Photo 11 38

Microstructure of quartz in a deformed type IIe vein. Crossed polars, long side of the photograph is 1.4 mm.

Photo 12 39

Microstructure of a quartz vein in a small shearzone (D4e1

) in an eclogite lens. Crossed polars, long side of the

photograph is 7 mm.

Photo 13 39

Core and mantle structure in a late intensively deformed quartz vein (D4e2

). Crossed polars, long side of the photograph

is 7 mm.

Photo 14 46

Fluid inclusions arranged along irregular planes in a recrystallised grain. Plane polarised light, length of scale bar

125 µm.

xvi

Table of figures

Figure 1 3

A Simplified geological map of the Central and Western Alps.

B Simpflied geological map of the northern part of the Western Alps.

C Simplified cross section through Figure 1B.

Figure 2 4

Simplified geological map of the vicinity of Lago di Cignana, based on 1.10000 mapping by Habermann (1992)

and Wagner-Zweigel (1993).

Figure 3 5

Simplified geological cross section through figure 2, showing the structure of the studied area.

Figure 4 6

The amount of individual reequilibration products plotted against the total amount of reequilibration products in

group 1 to 4 eclogites.

Figure 5 8

Compositions of clinopyroxene in eclogites from Lago di Cignana.

Figure 6 9

Compositional trends of zoned garnets in different eclogitic samples from Lago di Cignana.

Figure 7 11

Differences in phengite compositions in relation to grain size and position of the analyses in the grain for sample

Cig 91-1 and the compositions of phengites from other samples.

Figure 8 15

Drawing after a SEM image of a blue-green amp, ab symplectite at an omp-omp grain boundary.

Figure 9 17

Compositional differences of amphiboles in different textural position for all eclogite groups.

Figure 10 21

Histogram of temperatures calculated with the plagioclase-amphibole thermometer of Holland & Blundy (1994)

for ab-amp symplectites in group 1 to 4 eclogites

Figure 11 25

The composition of chlorite in relation to its microstructural position.

Figure 12 28

Microstructure of a group 1 eclogite.

Figure 13 29

Orientation of structural elements in eclogites, depicted in stereographic projections.

Figure 14 30

Histograms showing the abundance of measured angles between foliation and shortest dimension of minerals or

mineral aggregates for eclogites with different amounts of lower PT-replacement products.

xvii

Figure 15 31

Schematic diagram (not to scale) depicting orientation, crosscutting relations and aspect ratios of the different vein

types and their relation to orientation of foliation S1e and shearbands S2

e as seen on a horizontal plane.

Figure 16 32

Schematic sketch of mesoscopic structural relations between eclogites, greenschists and metasedimentary rocks at

Lago di Cignana.

Figure 17 35

Orientation of structural elements in the metasedimentary rocks, depicted in stereographic projections.

Figure 18 40

Several calibrations of the dynamically recrystallised grain size paleopiezometer for quartz.

Figure 19 42

Lattice preferred orientation of quartz (c-axes) in selected veins in eclogite, that underwent grain growth under low

differential stress after deformation (Bk 4,5,8,20,118) and a vein that deformed during D4e1

(Bk 119). Data are

presented as scatter plots and contour plots.

Figure 20 43

Lattice preferred orientation of quartz (c-axes) of veins deformed during D4e2

. Data are presented as scatter plots

and contour plots.

Figure 21 44

Lattice preferred orientation of quartz (c-axes) in veins subparallel to foliation S2s

. Data are presented as scatter

plots and contour plots.

Figure 22 45

Lattice preferred orientation of quartz (c-axes) in veins deformed in D3s

. Data are presented as scatter plots and

contour plots.

Figure 23 48

Melting temperatures against temperature of homogenisation for the fluid inclusions in the investigated samples

differentiated for the arrangement of the fluid inclusions.

Figure 24 49

Position of the isochores (equation of state of Brown & Lamb (1989) ) for the early and late fluid inclusions from

samples Bk 20 and Bk 100.

Figure 25 51

PT-d path for the exhumation of UHPM rocks of Lago di Cignana, Western Alps, Italy, modified after van der

Klauw et al., (1997).

Figure 26 55

Flow law „best choice 2“ of Paterson & Luan (1990) for dislocation creep in synthetically prepared wet quartzite

for geological relevant strain rates of 10-14 and 10-16 s-1.

Figure 27 56

Above: Cooling curve calculated for rocks of the Zermatt Saas-Fee zone.

Below: Decompression curve for the rocks of Lago di Cignana calculated by combining the cooling curve of the

Zermatt Saas-Fee zone and the PT-path of the rocks fom Lago di Cignana.

xviii

Figure 28 59

Schematic sketches illustrating the exhumation concept of Chemenda et al. (1995).

Figure 29 60

The plastic or Coulomb wedge in the concept of Platt (1986, 1987), with terms that describe the geometry of a

steady state wedge.

Figure 30 61

Tectonic evolution of the Western Alps after Platt (1987).

Figure 31 62

Schematic diagramm after Royden (1993) showing the response of the upper plate to different relative velocity

configurations of the subducting and overriding plate.

Figure 32 63

Simplified cross section illustrating successive positions and trajectories of identifiable points in the dynamic

scaled wedge model of Cowan & Silling (1978).

Figure 33 67

A tentative schematic sketch, illustrating some important points of the proposed exhumation scenario for the

UHPM rocks of Lago di Cignana.

The upper sketches show the configuration at UHPM conditions before exhumation.

The lower sketches show the configuration at the onset of exhumation.

Figure 34 70

A tentative schematic sketch, illustrating the proposed exhumation scenario for the UHPM rocks of Lago di Cignana

from depths of 25 km to ca. 10 km.

The upper sketches show the configuration just after break-off of the oceanic crustal slab.

The lower sketches shows the proposed exhumation scenario.

Appendix A

Figure A1 A-1

Distribution of the different lithologies at the southern shore of Lago di Cignana.

1

1 Introduction

Ultrahigh pressure metamorphic (UHPM) rocks have been described from a number of localities

(for reviews, see Schreyer, 1995; Harley & Carswell, 1995; Coleman & Wang, 1995). These crustal

rocks underwent metamorphism at depths well above the thickness of present-day crust, at

temperature-pressure ratios below 50 °C/100 MPa. The processes, during which such high pressures

at relatively low temperatures are produced, are generally accepted and a subduction mechanism

with thickening through thrusting in the overlying crust is usually postulated (e.g., Chopin, 1984;

Schreyer, 1995). The processes that returned UHPM rocks to the surface are still under discussion,

however (e.g., Platt, 1993; Harley & Carswell, 1995). Understanding of these processes constrains

kinematics and dynamics of convergent plate boundaries and several kinematic exhumation models

have been proposed (e.g., Platt, 1993; Chemenda et al., 1995; Davies & von Blanckenburg, 1995;

Thomson et al., 1998). To distinguish between these models, accurate information on P(ressure),

T(emperature), and structural evolution as well as unambigeous geochronological data for the UHPM

rocks must be available. For most UHPM rocks the outlines of the PT-paths are principally known

and continually improved (see Schreyer, 1995; Harley & Carswell, 1995), although the reconstruction

of complete PT-paths is hampered by the discontinuous record preserved in the rocks and the common

failure of rocks at attaining even small scale heterogeneous equilibrium during exhumation. Data

for the structural evolution of most UHPM terrains are scarce (see Michard et al., 1995), because

UHPM deformation fabrics and structures formed on the earlier part of the exhumation path are

seldom preserved, owing to intense distributed deformation under greenschist facies conditions.

The structural record acquired on the way to the surface provides vital information about the

exhumation process, however, and every proposed exhumation scenario should be based on an

analysis of this record (e.g., Wheeler, 1991; Henry et al., 1993; Michard et al., 1993 in Dora Maira

and Andersen et al., 1991, in south Norway). Geochronological data from several localities, indicate

that UHPM at depths of 100 km or more and a return to shallower crustal levels may take place in

a few million years (e.g., Tilton et al., 1991; Gebauer et al., 1997 in Dora Maira; Barnicoat et al.,

1995; Amato et al., 1999, in Zermatt Saas; Ames et al., 1996; Hacker & Wang, 1995 in Dabie Shan;

Shatsky et al., 1999 in Kazachstan).

This study concentrates on the exhumation of a small occurrence of UHPM oceanic crust at

Lago di Cignana, Valtournanche, Western Alps (Reinecke, 1991; Reinecke et al., 1994). Part of this

study, which deals with the petrologic, structural, and microstructural record of the metabasic rocks

at Lago di Cignana, was published in van der Klauw et al. (1997). The record of the metabasic rocks

will be correlated with the PT-record (Reinecke, 1995; 1998), and the (micro-)structural record of

the metasedimentary rocks and discussed in terms of state of stress, and mechanical behaviour

during successive stages of exhumation. These data provide the boundary conditions for a tentative

exhumation model for the UHPM rocks of Lago di Cignana.

2

2 Regional geology

The Alps are traditionally subdivided in four domains (Fig. 1A); the Helvetic and Penninic

domains both with mainly north vergent structures, derived from the European continent, respectively,

the European continent and oceanic crust; and the Austroalpine and Southalpine domains both

derived from the southern continent and with mainly north, respectively, south vergent structures

(e.g., Heim, 1922; Debelmas & Lemoine, 1970). The arrangement of these domains, with the

Austroalpine domain thrust on the Penninic domain and both thrust on the Helvetic domain, indicate

that convergence of the European plate and the Adriatic plate and SE directed subduction of

intervening oceanic crust, followed by continent-continent collision during the Cretaceous and

Tertiary, formed the Alps (e.g., Coward & Dietrich, 1989; Dewey et al., 1989; Polino et al., 1990).

Lago di Cignana is situated in the northern part of the Western Alps (Fig. 1B). The UHPM rocks

are part of the Penninic, Piemontese zone - a remnant of the former ocean. The Piemontese zone is

divided in the Combin zone, consisting mainly of calcschists (e.g., Deville et al., 1992) and in the

Zermatt Saas zone - a dismembered ophiolitic sequence - that is built up by peridotites, metabasalts

and subordinate oceanic metasedimentary rocks (e.g., Bearth, 1952; Barnicoat & Fry, 1986). The

UHPM rocks are part of the Zermatt Saas zone.

The mineral assemblages in the rocks of the Zermatt Saas zone reflect an eclogite facies meta-

morphic imprint of Early Tertiary age (52 ± 18 Ma, Bowtell et al., 1994; 40.6 ± 2.6 Ma, Amato et

al., 1999; 44.1 ± 0.7 Ma, Rubatto et al., 1998). The PT-conditions for this eclogite facies metamor-

phism have been estimated by several authors (Table 1). The large differences in the estimated PT-

conditions may reflect real differences in the metamorphic evolution of different parts of the Zermatt

Saas zone, but the discrepancies are for the earlier studies (Ernst & Dal Piaz, 1978; Oberhänsli, 1980)

certainly also due to the lack of well calibrated geothermobarometers at that time. The eclogite

facies mineral assemblages were partly reequilibrated during cooling and decompression (e.g.,

Meyer, 1983; Barnicoat & Fry, 1989). Locally an intense greenschist facies overprint developed

(Ernst & Dal Piaz, 1978; Barnicoat, 1988b). The K-Ar, Ar-Ar, and Rb-Sr ages of white micas range

from 45 to 30 Ma (Hunziker, 1974; Barnicoat et al., 1995). The oldest ages are interpreted as

Table 1

Pressure and temperature estimates of different authors for the high pressure metamorphism and laterreequilibration (exhum. P1; T1, exhum. P2; T2) of rocks from the Zermatt Saas zone.

3

cooling ages below the closure temperature of white mica (ca. 350 °C, Hodges, 1991). The younger

ages are interpreted as reset during later localised deformation (Barnicoat et al., 1995).

The rock units in the northern part of the Western Alps can be subdivided in units that experienced

an eclogite facies metamorphism (Zermatt Saas, Monte Rosa and parts of the Sesia zone) and units

Figure 1

A Simplified geological map of the Central and Western Alps.

B Simpflied geological map of the northern part of the Western Alps (modified after Ballèvre & Merle,1993). The arrow shows the approximate position of Lago di Cignana. Z-S = Zermatt-Saas.

C Simplified cross section through Figure 1B (modified after Ballèvre & Merle, 1993).

4

that experienced maximum pressures (< 1.4 GPa) of blueschist facies metamorphism (Grand Saint

Bernhard, Dent Blanche and Combin), during the alpine orogeny. In these last units, an early blueschist

facies metamorphic imprint (e.g., Ayrton et al., 1982; Desmons, 1992) is almost completely obliterated

by a greenschist facies overprint, associated with an usually penetrative ductile deformation (e.g.,

Wüst & Baehni, 1986; Dal Piaz & Ernst, 1978). Only for the Grand Saint Bernhard unit an age

estimate for the blueschist facies metamorphism is known (< 54 Ma, Monié, 1990). The later

greenschist facies overprint is estimated for all units to have occured between 45 - 35 Ma (Hunziker,

1986; Hunziker et al., 1989). Structures at the contacts between the blueschist units, indicate

juxtaposition of these units by NW-ward directed thrusting under greenschist facies conditions

(Mazurek, 1986; Wüst & Baehni, 1986; Ellis et al., 1989). The units with eclogite facies meta-

morphism experienced different maximum pressure and temperature conditions (e.g., Table 1; Chopin

& Monié, 1984) at different times. This shows that juxtaposition of these units did not occur at high

pressure conditions, as also suggested by the greenschist facies shearzones at the contacts between

the units (Ellis et al., 1989). A greenschist facies metamorphic overprint, estimated to have occurred

between 40 and 35 Ma (Chopin & Monié, 1984; Barnicoat et al., 1995; Inger et al., 1996), is locally

developed, often accompanied by penetrative ductile deformation (e.g., Williams & Compagnoni,

1983; Frey et al., 1976; van der Klauw et al., 1997).

The present day configuration, with the blueschist to greenschist facies metamorphic rocks on

top of the eclogite facies metamorphic rocks (Fig. 1C), developed between 36 and 30 Ma (Barnicoat

et al., 1995; Freeman et al., 1997), by SE directed thrusting of the blueschist facies rocks over the

eclogite facies metamorphic units, under lower greenschist facies conditions (Wheeler & Butler,

Figure 2

Simplified geological map of the vicinity ofLago di Cignana, based on 1.10000 mappingby Habermann (1992) and Wagner-Zweigel(1993).

Key: (1) eclogites and derived greenschists(Zermatt Saas zone), (2) UHPM metasedi-mentary rocks (Zermatt Saas zone), (3)serpen-tinised ultramafic rocks, (4)greenschists with minor calcschists (Combinzone), (5) calcschists with minorgreenschists and marbles (Combin zone), (6)dolomite-calcite marbles (exotic decollementsheet, cf. Dal Piaz, 1988), (7) Austroalpine(undifferentiated), (8) scree, moraine depositsand wetlands, (9) tectonic contact, (10)normal faults.

5

1993). The zircon fission track ages of approx. 33 Ma observed in all rock units in this part of the

Alps indicate that at this time all units exposed at the surface today were at temperatures of ca.

225 °C (Hurford et al., 1991). The different apatite fission track ages within some units, suggest

differential uplift and cooling histories for parts of these units between the Oligocene and the present

(Hurford et al., 1991).

2.1 The studied area

The studied area is situated south of Lago di Cignana, Valtournanche. The rocks in this area

belong to the Zermatt Saas zone, the Combin Zone, and the Dent Blanche zone. A simplified

geologic map of the area (Habermann, 1992; Wagner-Zweigel, 1993) and a simplified section are

shown in figures 2 and 3. The lithological divisions are comparable to those proposed by other

authors in this area (Dal Piaz, 1988; Marthaler & Stampfli, 1989; Vannay & Allemann, 1990).

In the area, the lowermost rocks are serpentinites of the Zermatt Saas zone. The serpentinites are

overlain by eclogites with a strong greenschist facies metamorphic overprint, usually, without pre-

servation of the eclogite facies mineral assemblage (Habermann, 1992). The top of these overprinted

eclogites consists of well preserved coesite bearing eclogites and metasedimentary rocks of the

Zermatt Saas zone. Most of the work was done on these eclogites, which were extremely well

exposed at the southern shore of the lake.

The rocks of the Zermatt Saas zone are overlain by the rocks of the Combin zone that can be

divided in three parts. The lowermost part of the Combin zone consists of greenschists with minor

amounts of calcschists. The upper part of the Combin zone is dominated by calcschists with only

minor amounts of greenschists and dolomitic marbles. Between these parts, locally dolomitic and

calcitic marbles occur that are considered a separate unit by Dal Piaz (1988). The uppermost rocks

in the studied area are the gneisses and schists of the Dent Blanche zone.

The occurence of serpentinites as small lenses within all units and as large lenses at the contacts

between the units, suggests that not only the contacts between the units are tectonic, but that also

within the units tectonic contacts occur.

Figure 3

Simplified geological cross section through figure 2, showing the structure of the studied area. Key as infigure 2.

6

Figure 4

The amount of individual reequilibration products plotted against the total amount of reequilibration productsin group 1 to 4 eclogites. Minor amounts (< 2 vol.%) of titanite (± ilmenite) rims around rutile in all eclogitesare omitted. Key: sympl = symplectite of blue-green amphibole and albite, czo = clinozoisite, amp grt =discontineous overgrowth of blue-green amphibole on garnet, amp gln = rims of blue-green amphibolearound glaucophane, chl = chlorite, and ab = albite.

3 The record in the metabasic rocks

In this chapter the record preserved in the metabasic rocks will be presented in two parts, first the

petrological part and second the structural part. The record preserved in the veins of the metabasic

rocks will be presented in chapter 5.

3.1 Petrology of the metabasic rocks - eclogites and greenschists

The metabasic rocks are presumed to be derived from basalts of former oceanic crust. This inter-

pretation is supported by bulk rock analyses of seven samples with different degrees of lower PT-

replacement (Table C2 in app. C) that invariably indicate MORB affinity, and by relic pillow

structures. This was already established for other localities in the Zermatt Saas zone (Dal Piaz et al.,

1981; Beccaluva et al., 1984; Pfeifer et al., 1989 and Bearth, 1959; Oberhänsli, 1982).

Two principal types of metabasic rocks can be distinguished. The first type comprises eclogites

and transformed eclogites, where the original eclogitic microstructure is still discernable owing to

pseudomorphic replacement. This holds true, even where the replacement to a lower PT-paragenesis

has gone to completion. The second type is represented by schistose metabasic rocks devoid of

high-pressure relics and is subsequently called greenschist. Greenschists constitute the minor portion

(estimated < 5 vol.%) of the metabasic rock in the studied area. They occur frequently at the contacts

between metasedimentary rocks and eclogite bodies and as m-sized lenses in both eclogitic and

metasedimentary rocks.

7

Table 2

The UHPM mineral assemblage and the lower PT-replacement products formed at their expense in thedifferent eclogite groups. sympl. = symplectite, aggr. = aggregate.

The eclogites can be classified in 5 groups, based on the degree of their lower PT-replacement

(Fig. 4 and Table 2):

Group 0 eclogites represent an idealised eclogite with perfectly preserved UHPM paragenesis.

In fact, such eclogites lacking any lower PT-replacement have not been found.

Group 1 eclogites appear macroscopically fresh, but a moderate amount (estimated 15-20 vol.%)

of replacement products is visible under the microscope.

Group 2 eclogites appear macroscopically darker green, because of partial replacement of

omphacite by a symplectite of amphibole and albite. Garnet is macroscopically still fresh,

however. Under the microscope between 20 and 55 vol.% of lower PT-replacement products

are visible.

In group 3 eclogites the replacement of garnet through an aggregate of biotite, chlorite, and

epidote is macroscopically visible. Between 55 and 85 vol.% of replacement products are

visible under the microscope.

In group 4 eclogites the replacement reactions have gone to completion and the amount of

replacement products reaches up to 100 vol.%.

For all eclogite groups, appearence and compositions of its minerals will be presented, followed

by a discussion of potential equilibrium paragenesis and PT-estimates. The minerals of the green-

schists will be treated together with group 4 eclogites.

8

Figure 5

Compositions of clinopyroxene in eclogites from Lago di Cignana. Only analyses from sample Bk 39 areshown; the core and rim analyses of Bk 39 are representative for omphacites from all samples studied. Key:ae = aegerine, jd = jadeite, quad = quadrilateral pyroxene.

3.1.1 Group 0 eclogites

In group 0 eclogites, clinopyroxene (omphacite), garnet, blue amphibole (glaucophane), clino-

zoisite I, zoisite, white mica, rutile, coesite, and apatite occur in all samples, whereas dolomite

occurs only in a few samples. Because no group 0 eclogites have been found, the mineral compositions

given are of minerals of group 1 eclogites, that are not in contact with lower PT-replacement products.

3.1.1.1 Mineral compositions

omphacite (omp)

The amount of omphacite ranges from 50 to 80 vol.% of the rocks. The omp grains are anhedral;

their shape preferred orientation partly defines the foliation. The grain size ranges from ca. 40 µm

for matrix grains, to ca. 400 µm for grains in strain shadows and along shearbands. The matrix omp

often shows a patchy extinction due to compositional inhomogenities. Grain boundaries between

omp grains are serrated. Some of the larger grains have slightly blueish anomalous interference

colours.

The omp composition in all samples (Fig. 5, Table C3 in app. C) and within a single sample

varies between Na(0.4-0.6)

Ca(0.4-0.6)

Mg(0.28-0.48)

Fe2+(0.03-0.14)

Al(0.36-0.56)

Fe3+(0-0.14)

Si2O

6. Mean composition for

all samples is close to Na0.53

Ca0.47

Mg0.38

Fe2+0.09

Al0.47

Fe3+0.06

Si2O

6. The composition appears to be

unrelated to the kind of adjacent mineral. Individual grains are homogeneous or consists of an

irregular patchwork of domains with slightly different composition, but generally, do not show a

regular zoning pattern. The boundaries between these domains are sharp. Commonly, omp inclusions

in garnet have similar compositions as matrix omp. Only in samples Bk 39 and Cig 91/40, the

9

Figure 6

Compositional trends of zoned garnets in different eclogitic samples from Lago di Cignana. Key: c = coreposition, r = rim position, adr = andradite, alm = almandine, grs = grossular, prp = pyrope, sps =spessartine.

aegerine content in inclusions is slightly larger and the jadeite content in the inclusions is slightly

smaller than in the matrix (Fig. 5).

garnet (grt)

Garnet occurs as euhedral porphyroblasts of up to 1 cm in diameter. The amount of grt ranges

from 10 to 20 vol.% of the rock. The cores of garnets contain abundant inclusions of omp, quartz

single crystals, and composite clinozoisite/epidote; paragonite; and titanite inclusions - pseudomorphs

after lawsonite (Bearth, 1959). In the rim of grt inclusions occur less frequently and are smaller.

They consist of omp, rutile and rarely very small (< 10 µm) quartz pseudomorphs after coesite.

Garnets are almandine rich (50-65 mol%), with appreciable amounts of pyrope (10-35 mol%)

and grossular components (10-35 mol%) and only minor (< 5 mol%) amounts of spessartine and

andradite components (Table C4 in app. C). Between the samples, compositions differ mainly in

the amounts of pyrope and grossular component (Fig. 6). The compositional zoning pattern of

garnets from different samples is similar (Fig. 6). The core of grt is relatively grossular rich. Towards

the rim the grossular component decreases and the pyrope and almandine components increase.

The compositional trend changes abruptly in the outer rim, with a relative decrease in almandine

component and an increase in pyrope component. The highest pyrope content occurs in the grt rim.

This change in composition trend, coincides with the change from inclusion rich core to inclusion

poor rim (Photo 3, Fig. 12).

glaucophane (gln)

The amount of gln ranges between 5 to 15 vol.%. The grains are subhedral; their shape preferred

orientation partly defines the foliation and stretching lineation. Grain sizes range from 50 µm in

10

sections perpendicular to c-axis to 500 µm parallel to c-axis. The composition (Table C5 in app. C)

differs slightly between the samples, varying between

(Na0-0.1

,K0-0.1

)(Na1.55-1.90

,Ca0.10-0.45

)(Fe2+0.55-1.00

,Mg2.00-2.45

,Al1.60-1.85

,Fe3+0.10-0.30

)2(Si7.70-7.95

,Al0.05-0.30

)O22

(OH)2.

Within a sample, the compositional variation is small and gln grains have a homogeneous

composition.

clinozoisite I (czoI)

Clinozoisite I amounts to < 10 vol.% of the rock. The grains size is up to 200 µm, the grains are

subhedral and their shape preferred orientation partly defines foliation and stretching lineation. The

composition lies between Ca2Fe3+

(0.26-0.50)Al

(0.50-0.74)Al

2Si

3O

8(OH) with the smallest Al

2Fe3+ epidote

component in the cores of larger grains, increasing towards the rim (Table 6C in app. C). Differences

in Al2Fe3+ epidote component in relation to the adjacent mineral are not observed. Between samples,

the range in Al2Fe3+epidote component differs slightly (Table C6 in app. C).

zoisite (zoi)

The amount of zoi is in the order of 3 vol.% of the rock. It is present as large (up to 3 mm)

anhedral grains with a patchy extinction and as smaller (< 50 µm) subhedral grains with a homo-

geneous extinction. The shape preferred orientation of the zoi aggregates partly defines foliation

and stretching lineation. Large grains have numerous randomly orientated white mica inclusions.

Composition varies between Ca2Fe3+

(0.10-0.15)Al

(0.85-0.90)Al

2Si

3O

8(OH) (Table C7 in app. C), with the

higher Al2Fe3+ epidote component in contact with czoI.

white mica

The white micas in group 0 eclogites are paragonite (pg) and phengite (phe) and usually cannot

be distinguished optically. The presence of pg or phe was established with powder X-ray diffraction.

In most samples pg is the only white mica, in some samples powder X-ray diffraction showed the

presence of both pg and phe, however. Further investigation with the electron microprobe, indicated

that in these cases the white mica generally consists of pg with phe intergrowths; the width of the

phe layers is below the beam size of the microprobe (about 5 µm). Only a few samples have phe as

the only white mica.

paragonite (pg)

The amount of pg ranges from 4 to 8 vol.% of the rock. Pg grains are subhedral and their shape

preferred orientation partly defines the foliation. Grain size is about 40 µm. The composition varies

slightly around (Na1.9

,K0.1

)Al4[Si

6Al

2O

20](OH)

4. Pg in phe bearing samples can have up to 15 mol%

of phe solid solution (Table C8 in app. C).

phengite (phe)

The amount of phe can amount to ca. 10 vol.% of samples, where it is only white mica. Phe is

present as small (< 40 µm) grains in the matrix and as large (about 400 µm) porphyroblasts. The

grains of both varieties are subhedral and their shape preferred orientation partly defines the foliation.

The large phe have compositions (Fig.7, Table C9 in app. C) varying between

11

Figure 7

Differences in phengite compositions in relation to grain size and position of the analyses in the grain forsample Cig91-1 and the compositions of phengites from other samples.

(K0.94-0.98

,Na0.03-0.05

)(Mg0.40-0.47

,Fe2+0.02-0.07

)(Al1.40-1.46

,Fe3+0.03-0.08

)(Si3.45-3.51

,Al0.49-0.55

)O10

(OH)2. Similar

composition are found in a few small matrix phe. Most small matrix phe and the rims of the large

phe have compositions (Fig.7, Table C9 in app. C) varying between

(K0.89-0.94

,Na0.08-0.12

)(Mg0.29-0.35

,Fe2+0-0.04

)(Al1.50-1.56

,Fe3+0.08-0.14

)(Si3.28-3.38

,Al0.62-0.72

)O10

(OH)2. Which phe

composition belongs to the UHPM mineral paragenesis is not clear, because phe of both compositions

occurs in contact with UHPM minerals as well as with late PT-replacement products.

rutile (rt)

Rutile amounts to up to 2 vol.% of the rock. The grains are anhedral, rounded and about 30 µm

in size. In one sample (Bk 8) mm-sized anhedral rt grains occur. Composition is TiO2 without

significant amounts of other elements (Table C10 in app. C).

apatite (ap)

Apatite amounts to 0.5 vol.% of eclogitic rocks and is present as anhedral rounded grains. Its

grainsize is up to 50 µm, in some quartz veins large 5 mm sized ap grains occur, however. Ap

compositions were not analysed.

dolomite (dol)

Dolomite occurs only in metabasic rocks that are rich in gln and white mica and are considered

to be derived from pillow rims or interpillow material (e.g., Oberhänsli, 1982; Barnicoat, 1988a).

The amount of dol is below 4 vol.% of the rock. Dol is present as small (< 40 µm) anhedral grains.

and often occurs in elongated aggregates of max. 0.5 cm in length. The shape preferred orientation

of these aggregates partly defines the foliation. It also occurs as approximately equidimensional

aggregates in strain shadows at grt. Dol is easy distinguished optically from late calcite, due to

12

Photo 2

Coesite inclusion in omp, with a small rim of quartzbetween cs and omp. Note, that the diameter of theinclusion is more than half the diameter of theincluding omp grain. Plane polarised light, length ofphotograph 1.4 mm.

Photo 1

Typical coesite inclusion in omp with a small rim ofquartz between omp and cs. Note the cracks in omp,radiating away from the inclusion. Plane polarisedlight, length of photograph 1.4 mm.

numerous fine grains of an opaque mineral, resulting from the oxidation of the ankerite component

in dol, that are present along its cleavage planes. Dol is considered part of the UHPM mineral

assemblage, because it occurs in contact with all other UHPM minerals and has inclusions of gln

and rt. The composition varies between Ca(Mg0.75-0.80

Fe0.25-0.20

)(CO3)

2, with minor (< 2 mol%) amounts

of Mn substituting for Mg and Fe (Table C11 in app. C).

coesite (cs)

Coesite is found as inclusions in omp (up to 30 µm) and possibly in grt rims (< 10 µm). The cs

inclusions have the typical characteristics described by Chopin (1984) with radial cracks in the host

mineral and a rim of columnar quartz between cs and the host mineral (Photos 1, 2). Cs occurs as

colourless to slightly greenish grains with higher relief as the surrounding quartz. In several inclusions

in omp, the presence of cs was unequivocally proven with the electron microprobe, that showed a

SiO2 composition for phases in the inclusions and, respectively, blue and yellow luminesence colours

for cs and quartz (Schulze & Helmstaedt, 1988). The cs in the two small inclusions in grt could not

unequivocally be identified.

13

3.1.1.2 Mineral paragenesis and PT-estimates

All minerals of group 0 eclogites (omp, grt, gln, czoI, pg, zoi, cs, rt, and ap, with in some

samples that will not be discussed, dol and phe), with exception of gln and zoi, can be found

occuring in mutual contact, although lower PT-replacement products always occur at contacts

between some minerals (e.g., blue-green amphibole between grt and gln). Paragonite is considered

part of the UHPM mineral paragenesis of group 0 eclogites, although experimental investigations

(e.g., Holland, 1979), indicate that pg is not stable at the PT-conditions of UHPM (2.7 GPa at

625 °C, Reinecke 1991; 1995). At these conditions, pg should have reacted to jadeite (jd component

in cpx) and kyanite (Holland, 1979). However, kyanite has not been observed in the metabasic

rocks at Lago di Cignana and pg occurs without UHPM reaction textures in direct contact with the

other minerals of the UHPM paragenesis. Furthermore, pg occurs as inclusions in omp, that has the

same composition as omp with cs inclusions. Similar observations of the persistence of pg outside

its stability field are known from Dora Maira (Schertl et al., 1991) and from Dabie Shan (Okay, 1995).

That gln and zoi do not occur in mutual contact, but are always separated by other UHPM

minerals, suggests that in group 0 eclogites two local equilibrium assemblages, with slightly different

bulk rock compositions, occur. The first and most abundant assemblage consists of omp, grt, gln,

pg, czoI, cs, rt, and ap, the second assemblage consists of omp, grt, zoi, pg, czoI, cs, rt, and ap.

These assemblages are coupled by the reaction (in mol):

0.25 gln + 0.29 zo = 0.87 omp + 0.07 grt(rim) + 0.08 czoI + 0.14 pg + 0.07 cs/qtz + 0.22 H2O

calculated with the mineral compositions of sample Bk 39, which is representative for group 0

eclogites. Rutile and ap are the only Ti-, respectively, P-bearing minerals and, therefore, do not

appear in this reaction. A similar reaction is given by Reinsch (1977) and Ridley (1984), as the

reaction, that marks the temperature dependent transition from blueschist to eclogite in metabasic

rocks. This indicates that mm-scale compositional inhomogenities (the size of the smallest gln or

zoi domains) that were present in the blueschist precursor of the eclogite, were preserved during

UHPM.

The inhomogeneous composition of grt, czoI, and omp can be explained with partial equilibrium

that assummes that reaction with a disequilibrium phase is kinetically inhibited. The equilibrating

bulk composition is the original bulk composition minus the composition of the disequilibrium

phase (Loomis, 1983). In the case of the more or less concentrically zoned grt and czoI, it can be

argued that only the outer rim is in equilibrium with the other phases, and that the core region is no

longer part of the system, because of relatively slow intracrystaline diffusion in grt (e.g., Chakraborty

& Ganguly, 1990) and czoI at the temperature of 625 °C during UHPM. The variable omp

compositions cannot be attributed to partial equilibrium, however. Omphacite grains are either

homogeneous, or consist of irregular domains with different compositions. The formation of these

domains is attributed to localised compositional reequilibration during grain boundary migration

(chapter 3.2), due to deformation under changing PT-conditions. This process makes it impossible

to identify the omp composition in equilibrium with the other phases.

14

Table 3

Temperatures (at 2.7. GPa) calculated with different calibrations of the grt-cpx thermometer for somerepresentative grt and omp combinations. Key: E&G79 = Ellis & Green (1979), P85 = Powell (1985), K88= Krogh (1988), P&N89 = Pattison & Newton (1989) and A94 = Ai (1994)

PT-estimates

Equilibration temperatures for the UHPM mineral assemblage were obtained with garnet-

clinopyroxene Fe2+-Mg exchange thermometry (see appendix B for a discussion of the different

calibrations of the thermometer). The presence of cs inclusions in matrix omp and of small inclusions

of quartz (pseudomorphs after cs) in grt rims, indicates that grt rims must be combined with matrix

omp to obtain temperatures for the UHPM. The Powell (1985) calibration gives temperatures of

595 ± 35 °C (1 σ) for 27 grt (rim)-omp pairs from five samples, calculated at a pressure of 2.7 GPa.

The variation in exchange temperatures is larger within one sample (Table 3, Table B2 in app. B),

than between the samples. This large variation might have several causes:

* Analytical erors, that influence the calculation of the Fe2+ and Fe3+ content in grt and omp.

* The incomplete zoning pattern of grt. The Mg-richest rim of the normal zoned grt is often

missing, for example, where grt partly embays a matrix omp.

* The inhomogeneous omp composition in contact with the grt rim. As discussed earlier, it is

not possible to unequivocally determine the omp composition, that is in equilibrium with the

grt rim.

Analytical errors were minimised by measuring each mineral at least two times in direct contact

and by comparing these single analyses. Deviating analyses were discarded and temperatures were

calculated with the mean of the remaining analyses for every grt-omp pair.

To solve the other problems, digital element distribution maps (DEDM, Bernhardt et al., 1995)

were made of all garnets used for geothermometry. These maps show that a compositionally

homogeneous omp can be embayed in a zoned grt (Photo 3) and therefore, occurs in contact with a

range of grt compositions. The DEDM do not show a reversal of the prograde compositional zoning

trend in grt at grt-omp interfaces. Therefore, reequilibration of the Fe2+-Mg exchange on the

exhumation path and diffusive relaxation in grt rim and omp rim can be excluded. The impossibility

to define unique grt and omp equilibrium compositions, indicates that during UHPM Fe2+-Mg

exchange equilibrium between grt and omp was not reached at all grt-omp interfaces.

15

Photo 3

A digital element distribution map for Mn in grt. Mn-content decreases from green-yellow in the core overorange to pink and blue in the rim. Black islands ingarnet are mostly omp inclusions. Note in the lowerright and upper left corner of the grt, omp inclusionsin contact with grt core composition and grt rimcomposition. Length of the picture ca. 5 mm.

Figure 8

Drawing after a SEM image of a blue-green amp, absymplectite at an omp-omp grain boundary.


In group 1 eclogites several minerals have formed as partial replacement products of the UHPM

mineral assemblage (Table 2). These replacement minerals are restricted to specific UHPM minerals

and microstructural sites. A symplectite of albite and blue-green amphibole often replaces omp

along cracks and grainboundaries (Fig. 8). Blue-green amphibole develops as rims around gln

(Photo 4), at contacts of grt with pg and gln and is often also present at grt in contact with other

UHPM minerals and along cracks in grt. In phe-bearing samples a green-brown mica occurs as

lower PT-replacement product between grt and phe. Rims of ilmenite and/or titanite develop around

rt. Clinozoisite II partly replaces zoi and pg. Quartz replaces cs and in dol bearing samples, calcite

partly replaces dol.

The relative amounts of these replacement products are similar in all group 1 samples (Fig. 4).

Only during this replacement stage irregular overgrowths of blue-green amphibole formed around

grt and gln. During later replacement stages, the amount of these amphiboles remained constant, as

long as these could be recognised from their microstructural position (Fig. 4). Therefore, this

replacement stage is considered common to all eclogite groups.


albite (ab)

Albite amounts to between 50 and 70 vol.% of the symplectite that replaces omp. This symplectite

amounts to between 8 and 12 vol.% of group 1 eclogites. Albite forms grains of up to 50 µm in

16

Photo 5

B(ack)S(cattered)E(lectron) photograph of the rim ofblue- green amp around gln. Different shades of grayin the rim suggest slight compositional differencesin the blue-green amp.

Photo 4

Glaucophane rimmed by blue-green amp (amp gln)in a matrix of omp and rt with titanite (ttn) rims. Planepolarised light, long side of the photograph is 1.4 mm.

diameter that include the smaller amphibole grains. The anorthite (an) component of ab is below

5 mol% (Table C13 in app. C).

blue-green amphibole (amp)

Blue-green amphibole in group 1 eclogites can be divided in three groups with different micro-

structural positions and compositions (Fig. 9):

1. amphibole rims around garnet

2. amphibole rims around glaucophane

3. amphibole in symplectite

1. amphibole rims around garnet.

The amount of this amp ranges from 2 to 3 vol.% in group 1 and 2 eclogites. In group 3 and 4

eclogites with partly replaced grt, the amp around garnet is difficult to distinguish from other

amphiboles and its amount becomes less. This amp is present as thin (max. 30 µm) discontinuous

rims around grt and along fractures in grt. The grains are anhedral and up to 100 µm in length. The

17

Figure 9

Compositional differences of amphiboles in different textural position for all eclogite groups. Amp at grtand at gln only occur in group 1 and 2 eclogites, non pseudomorphic amphiboles and vein amphiboles onlyoccur in group 3 and 4 eclogites. Na

M1 is Na in the M1-position, pfu is per formula unit.

composition (Table C14 in app. C) ranges between magnesian-hastingite and magnesian-hastingitic-

hornblende (amp names after Leake, 1978).

2. amphibole rims around glaucophane

The amount of this amp ranges from 2 to 3 vol.% in group 1 and 2 eclogites. In group 3 and 4

eclogites, gln is completely transformed, and this amp cannot be identified. At grt-gln contacts a

transition in composition from amp around gln to the amp around grt is found. Back scattered

electron (BSE) images of amp rims indicate that these rims consist of patches (few µm2 in size)

with different compositions (Photo 5). The size of these patches is close to the beam size of the

microprobe and this is reflected by the highly variable measured compositions (Fig. 9, Table C15 in

app. C) for these amphiboles, between barroisite, actinolite and magnesio-hornblende (amp names

after Leake, 1978).

3. amphibole in symplectite (ampI)

The ampI comprises between 30 and 50 vol.% of the ab-amp symplectites (Fig. 8) that are the

lower PT-replacement products of omp. The grains are subhedral and small (< 20 µm). The

composition (Table C16 in app. C) ranges from magnesian-hornblende to actinolitic-hornblende

(amp names after Leake, 1978). In direct contact with quartz, ampI is always actinolite. This suggests

that after formation of the symplectite from omp, the ampI in contact with quartz has reequilibrated

according to the simplified reaction:

18

edenite + quartz = tremolite + albite (Holland & Blundy, 1994).

This is supported by the observations that i) symplectites after omp in quartz veins comprise a

larger amount of ab and ii) ampI adjacent to quartz aggregates is an actinolite at the symplectite-

quartz contact, but an actinolitic hornblende at the symplectite omp contact.

titanite (ttn)

Titanite amounts to up to 1.5 vol.% of group 1 eclogites. It forms anhedral grains up to 50 µm in

size, often with minor rt and ilmenite preserved in its core and also occurs as composite inclusions

with pg and czo in the core of garnets. Its composition is approximately Ca(Ti0.95

Al0.05

)

[SiO4](O,OH,F) (Table C17 in app. C).

ilmenite (ilm)

Ilmenite amounts to 0.5 vol.% of the rock. It forms small (< 20 µm) anhedral grains that usually

occur as discontinuous rims around rt. Ilmenite has also rarely been observed along cracks and as

inclusions in grt. The ilm composition in contact with rt is (Mg0.2

, Mn0.03

, Fe2+0.95

)TiO3, in grt its

composition (Mg0.01

, Mn0.1

, Fe2+0.89

)TiO3 is similar along cracks and in inclusions (Table C18 in

app. C).

clinozoisite II (czoII)

Clinozoisite II amounts to up to 3 vol.% of group 1 eclogites. It occurs as discontinuous rims

around large czoI grains in contact with lower PT-replacement products and as small (about 20 µm)

euhedral grains in aggregates of white mica. The composition of czoII (Table C6 in app. C) lies

between Ca2Fe3+

(0.40-0.55)Al

(0.45-0.60)Al

2Si

3O

8(OH). Between samples, the range in Al

2Fe3+epidote

component differs slightly.

quartz (qtz)

Quartz amounts to up to 2 vol.% of metabasic rocks. It is present as anhedral grains of max.

40 µm or as aggregates of several grains of up to 100 µm in size. It is also present as small (< 30 µm)

grains along shearbands and as vein filling material. Quartz is always completely surrounded by

lower PT-replacement products. Quartz also occurs as monomineralic inclusions in grt and seldom

in omp.

calcite (cal)

Calcite is present in only few samples of the metabasic rocks. In one group 1 eclogite, cal occurs

as a rim around dol grains and it amounts to < 2 vol.% of the rock. The composition varies slightly

between (Fe, Mg, Mn)<0.1

Ca>0.9

CaCO3 (Table C12 in app. C). Cathodoluminesence (CL) investigations

of cal, have shown that the CL colours depend on the relative amounts of Mn and Fe (Marshall,

1988). High Mn- and low Fe-contents result in bright yellow CL colours; High Fe- and low Mn-

contents result in a dark CL colour. In the group 1 eclogites, the Mn-content of cal is almost constant

at approx. 1 mol% (Table C12 in app. C). The Mg- and Fe-content is positively correlated. Therefore,

the CL colours of cal give an indication of the relative amounts of Mg and Fe in calcite. Dark

19

Photo 7

Late replacement of grt by chl and epidote (czoV).Crossed polars, long side of the photograph is 7 mm.

Photo 6

Cathodoluminescence photograph of cal in a dolomitedomain. Different shades of orange (cal1, cal2)represent cal with different amounts of Mn, Mg andFe. Long side of the photograph is 3.8 mm.

orange-red CL colours (high Mg- and Fe-contents) occur at the rim zone away from dol in the cal

overgrowths on dol, whereas towards dol the cal becomes brighter orange (Photo 6). In contact with

dol, cal has yellow-orange CL colours (low Mg- and Fe-contents). This change in CL colours is

present in all carbonate aggregates, but the absolute amounts of Mg and Fe differ slightly between

the aggregates.

green-brown mica

This green-brown mica occurs as small anhedral grains between phe and grt. It amounts to

< 1 vol.% and its composition is approximately (Na0.06

K0.94

)(Mg1.23

Fe1.18

)Al1.8

Si2.67

O10

(OH)2

(Table C19 in app. C).


In the group 1 eclogites several minerals have formed as partial replacement products of minerals

of the UHPM assemblage. The amount of these replacement products is similar in all group 1

eclogites, independent of the relative amounts of the UHPM minerals. This suggests that these

replacement products formed simultaneous. However, the minerals of this first replacement stage

20

Table 4

Pressures (at 550 °C) calculated with the jd (in omp)+qtz=ab barometer of Holland (1980), using the methodof Holland (1990) for the calculation of jadeite activity in omp, for extreme omp compositions. Key:X(jd,acm,diop,hed) = resp. jadeite, acmite, diopside and hedenbergite component in cpx, a(jd) = jadeiteactivity, max. X(xx) = cpx analysis with highest xx component, min. X(xx) = cpx analysis with lowest xxcomponent, the analyses with min. X(jd) and min. X(diop) have also, resp., max. X(diop) and max. X(hed).

are not an equilibrium paragenesis, because three amp at different textural sites have different

compositions. The observation, that the lower PT-replacement products are restricted to specific

minerals of the UHPM mineral assemblage (Table 2), suggests local equilibrium. The local

equilibrium domains were defined by the different chemical compositions of the UHPM minerals

and the size of the domains was the grain size of the UHPM minerals.

PT-estimates

Pressures and temperatures for the onset of this lower PT- replacement can be obtained from two

independent domains: the omp (symplectite) domain present in all samples and the carbonate domain

present in one sample only.

The omphacite domain

The reaction inferred for this domain is:

omphacite = amphibole + albite

This reaction can be used to calculate temperatures and pressures according to partial reactions

(discussion of these thermo-barometers in Appendix B):

jadeite (in omp) + quartz = albite (barometer, Holland, 1980)

edenite (in amp) + quartz = tremolite (in amp) + albite (thermometer, Holland & Blundy, 1994).

A prerequisite, to obtain equilibrium temperatures and pressures with these reactions for omp

decomposition, is that qtz and omp occurred in mutual contact. Quartz is only seldom found in

partly replaced eclogites and never in mutual contact with omp. Therefore, the calculated pressures

of 1.2 to 1.3 GPa (Table 4, Table B6 in app. B) and temperatures of 525-575 °C (Fig. 9A, Table B3

in app. B) are maximum pressures and temperatures for the omp decomposition reaction. When qtz

is present, it occurs in veins or it is completely surrounded by lower PT-replacement products. This

21

Figure 10

Histogram of temperatures calculated with the plagioclase-amphibole thermometer of Holland & Blundy(1994) for ab-amp symplectites in group 1 to 4 eclogites, calculated at a pressure of 1.2 GPa. N is number ofsamples

suggest that the decomposition reaction ceased, when all qtz present in the reaction domain was

used up. Another suggestion is that the reaction ceased, when qtz was no longer available in the

reaction domains due to its rim of lower PT-replacement products.

The large range of temperatures (Fig. 10, Table B3 in app. B), partly results from the inhomo-

geneous compositions of educt and product phases. Omphacite has 0.6 > Xjd > 0.45 and, therefore,

the onset of symplectite formation will occur at different pressures and temperatures. Consequently,

the varying ampI compositions reflect different formation temperatures. The varying ampI composi-

tions could also result from contamination of the analyses of these fine grained ampI with ab, re-

sulting in higher Si, Al and Na content in the ampI and in a lower calculated formation temperature.

The carbonate domain

Pressure and temperature estimates for this domain are obtained with the cal-dol solvus thermo-

meter (Anovitz & Essene, 1987, see Appendix B for discussion), from calcite in contact with

dolomite, which shows temperatures of 575-450 °C for cal in aggregates with dol (Table 5, Table B5

in app. B). Combined CL and electron microprobe investigations of the carbonate aggregates, show

that the calculated temperature depends on the position in the carbonate aggregate (Photo 6). This

suggests that the reaction of dol to cal started at the rim of the dol grain and that the earliest cal

formed in equilibrium with dol was relatively Mg and Fe rich (dark orange-red CL colours). Further

reaction of dol to cal occurred at the interface between the earlier formed cal and dol. This new cal,

which formed in equilibrium with dol, was less Mg and Fe rich (orange CL colours). Again further

reaction occurred at the interface between the younger cal and dol. The cal formed at this stage in

equilibrium with dol, was relatively Fe and Mg poor (yellow-orange CL colours). This zoning trend

22

Table 5

Temperatures calculated with the calcite-dolomite thermometer of Anovitz & Essene (1987) for somerepresentative cal analyses in domains with different cl colours. T1 and T2 are, resp., calculated for systemCa2+-Mg2+ and Ca2+-Mg2+-Fe2+.

is contrary to a trend expected for diffusional reequilibration for cal in contact with dol. This means

that temperatures calculated with the compositions of cal with dark orange-red CL colours (575-

525 °C) mark the upper limit for the onset of the reaction of dol to cal.

Because aragonite does not contain appreciable amounts of Mg, Fe and Mn, the Mg-Fe-Mn rich

cal must have formed in the stability field of cal. Therefore, the maximum pressure for the onset of

the reaction of dol to cal at 550 °C, is limited to 1.1-1.2 GPa by the aragonite-calcite univariant

equilibrium (Johannes and Puhan, 1971).

The PT-conditions for the onset of lower PT-replacement in group 1 eclogites obtained from

two independant domains are estimated at P < 1.2 GPa and T < 550 °C.


In group 2 eclogites the mineral assemblage is the same as in group 1 eclogites, but the amounts

of ab-amp symplectites, czo and ttn formed at the expense of omp and gln, pg and rt, respectively,

are increased. In carbonate bearing samples, cal is the only carbonate mineral present.


albite (ab)

In group 2 eclogites ab is present in symplectite that amounts to up to 45 vol.% of group 2

eclogites. The only difference from ab in group 1 eclogites is the grain size of up to 80 µm.

amphibole in symplectite II (ampII)

Amphibole II occurs in the ab-amp symplectites, that are the lower PT-replacement products of

omp and gln. The ampII grains are subhedral and often slightly larger (< 30 µm) than ampI grains in

group 1 eclogites. However, it is not unequivocally possible in a group 2 eclogite to distinguish

between ampI and ampII. The composition of amphibole (ampI + ampII) in group 2 eclogites (Fig. 9,

Table C16 in app. C) ranges from magnesio-hornblende to actinolite (amp names after Leake,

1978).

23

clinozoisite III (czoIII)

Clinozoisite III amounts to up to 3 vol.% of group 2 eclogite and occurs as discontinuous rims

around large czoI and czoII grains in contact with lower PT-replacement products, and as rims

around the smaller euhedral czoII grains in aggregates of white mica. The composition (Table C6 in

app. C) lies between Ca2Fe3+

(0.45-0.60)Al

(0.40-0.55)Al

2Si

3O

8(OH).

titanite (ttn)

Titanite amounts to up to 2 vol.% of the rock in group 2 eclogites. The ttn formed during this

stage of lower PT-replacement has the same composition as earlier formed ttn and can not be

distinguished from earlier formed ttn.

calcite (cal)

Calcite occurs as untwinned anhedral grains of up to 4 mm in their longest dimension, interpreted

to be pseudomorphs after dol aggregates and as small (< 30 µm) anhedral grains along shearbands.

Calcite in group 2 and later eclogites has lower amounts of Mn, Fe and Mg substituting for Ca than

cal in group 1 eclogites (Table C12 in app. C), but because of the differing amounts of Mn in the cal,

the CL colours can no longer be directly correlated with the amount of Mg and Fe in cal.

3.1.3.2 Mineral paragenesis and PT- estimates

In the group 2 eclogites the mineral assemblage is similar to the assemblage in group 1 eclogites.

Some of the lower PT-replacement products that formed during this stage, however, have compo-

sitions different from similar replacement products in group 1 eclogites. The replacement minerals

that formed earlier did not change their composition in these samples. Therefore, the compositional

range of lower PT-replacement products is larger in group 2 eclogites than in group 1 eclogites. The

localised occurrence of the newly formed minerals, suggest that similar to group 1 eclogites, the

reaction products were in local equilibrium only. Therefore, the size of the equilibrium domains is

still similar to the grain size of the UHPM minerals.

PT-estimates

In group 2 eclogites dol is no longer present and therefore, the cal-dol thermometer cannot be

applied. Temperatures for this lower PT-replacement stage can be obtained from the omp (sym-

plectite) domain with the Holland & Blundy (1994) plagioclase-amphibole-quartz-thermometer.

Temperatures range from 500 to 575 °C (Fig. 10, Table B3 in app. B). This large range in calculated

temperatures is due to the presence in group 2 eclogite samples of 2 generations of symplectitic

amp (Fig. 9). Higher temperatures are calculated with amphiboles inherited from the earlier lower

PT-replacement stage and lower temperatures (500-525 °C) are calculated with newly formed more

actinolitic amphiboles. Because ampII is coarser grained than ampI, contamination of these analyses

with albite is improbable. Therefore, the higher Si-content in ampII compared to ampI suggests

decreasing temperatures (500 -525 °C) during later replacement in group 2 eclogites. A pressure

estimate for this stage is not possible.

24


In group 3 eclogites the replacement of gln and omp through ab-amp symplectites is completed.

The remaining pg is partly replaced by chlorite. Garnet is partly decomposed to an aggregate of

chlorite, dark mica, epidote (czoIV) and ab (Photo 7). Symplectitic amp partly grows to a coarser

amphibole.


albite (ab)

Albite occurs in two textural positions in group 3 eclogites. It occurs in symplectites that amount

to up to 55 vol.% of group 3 eclogites. This ab differs only in its grain size of up to 120 µm from

earlier formed ab in symplectite. Albite also occurs in the aggregates of several minerals replacing

grt. This ab forms anhedral grains of up to 100 µm in size and has between 8 and 10 mol% an

(Table C13 in app. C).

amphibole in symplectite III (ampIII)

The ampIII grains are subhedral with a grainsize larger (< 50 µm) than ampI and ampII in group 1

and 2 eclogites. In a group 3 eclogite, it is not unequivocally possible to distinguish between ampIII

and earlier ampI and ampII. The composition of amphibole (ampI + ampII + ampIII) in group 3

eclogites ranges (Fig. 9, Table C16 in app. C) from magnesio-hornblende to actinolite (amp names

after Leake, 1978), with a larger number of actinolites than in group 2 eclogites.

coarse amphibole

This amphibole forms large (up to 100 µm) subhedral grains and amountsto up to 5 vol.%. It

develops at the cost of small symplectitic amphiboles and has inclusions of ab, czo and ttn. The

composition (Table C20 in app. C) varies from actinolitic hornblende to actinolite (names after

Leake, 1978).

clinozoisiteIV (czoIV)

Clinozoisite IV amounts to nearly 3 vol.% and occurs in two textural positions. It occurs as

discontinuous rims around earlier czo grains with a composition (Table C6 in app. C) between

Ca2Fe3+

(0.50-0.70)Al

(0.30-0.70)Al

2Si

3O

8(OH) and also as large, up to 80 µm, anhedral grains in mineral

aggregates replacing grt, with a composition between Ca2Fe3+

(0.62-0.78)Al

(0.22-0.38)Al

2Si

3O

8(OH).

chlorite (chl)

Chlorite amounts to up to 5 vol.% of group 3 eclogites. It is present as randomly oriented stacks

in large (up to 1 cm) aggregates. The aggregates are approximately circular for chl formed at the

expense of grt and “stick” like for chl formed at the expense of white mica. The composition varies

between (Mg4.5-6.5

,Fe2+1.7-4.0

,Fe3+0.80-0.95

,Al2.1-2.5

)(Si5.3-5.6

,Al2.4-2.6

)(OH)16

(Table C21 in app. C) and depends

on textural position. The chl formed at the expense of white mica has XMg

, Mg/(Mg+Fe2+) between

0.7-0.8, whereas chl formed at the expense of grt has XMg

between 0.5-0.6 (Fig. 11). In the matrix

chl, that cannot be attributed to white mica or grt, has intermediate XMg

.

25

Figure 11

The composition of chlorite in relation to its microstructural position. pfu, per formula unit.

dark mica

This dark mica amounts to up to 1.5 vol.% of the rock and occurs as a fine grained intergrowth

with chlorite in aggregates replacing garnet. It was not possible to obtain reliable analyses of this

dark mica.


In the group 3 eclogites the mineral assemblage is the assemblage of group 1 and 2 eclogites

with chlorite and a dark mica added. Some of the replacement products formed during this stage

have a different composition from similar, earlier formed, replacement products. However, the

minerals that formed during these earlier stages retained their composition (e.g., Fig. 9). The localised

occurrence of the newly formed minerals, suggest that similar to group 1 and 2 eclogites, the reaction

products were in local equilibrium only. However, the presence of chlorite with intermediate

composition and the growth of large amphiboles, indicate that at least locally the size of the

equilibrium domains was larger than the grain size of the original UHPM minerals.

PT-estimates

Temperatures for this replacement stage can be obtained from the omp (symplectite) domain

with the Holland & Blundy (1994) plagioclase amphibole thermometer. Calculated temperatures

range from 475 to 575 °C (Fig. 11, Table B3 in app. B). Some of the ampIII has a composition with

Si > 7.7 per formula unit (pfu) and is outside the compositional limit of the thermometer (Holland

& Blundy, 1994). These compositions, however, still point to formation temperatures below 475 °C.

The large range in calculated temperatures is, as in group 2 eclogites, due to preservation of earlier

formed amp(I and II). Therefore, a temperature below 500 °C is a reasonable estimate for stage 3

replacement. A pressure estimate for this stage is not possible.

26

3.1.5 Group 4 eclogites and greenschists

In group 4 eclogites the replacement of the UHPM mineral assemblage goes to completion and

a new paragenesis comprising chl, green amp, czoV, ttn, and ab has formed. The earlier replacement

products that formed pseudomorphs after the UHPM paragenesis and thereby, preserved the original

microstructure, are partly replaced by the new paragenesis; hence, the original microstructure is

largely obscured. The greenschists are rocks, where replacement and recrystallisation have gone to

completion. The composition of the greenschist minerals is the same as the minerals of the group 4

eclogites.


albite (ab)

Albite amounts to < 50 vol.% of the rock. It occurs in symplectite, in the aggregates replacing

grt, and as latest replacement product of remaining white mica. Locally, cm-sized poikiloblasts of

ab occur. In symplectite ab has < 5 mol% an, in other position an contents are between 5 and

10 mol% (Table 13C in app. C).

coarse amphibole

This amphibole forms large (up to 100 µm) subhedral grains and amounts to up to 10 vol.%. It

develops at the cost of small symplectitic amphiboles and has inclusions of ab, czo and ttn. The

composition (Table C20 in app. C) varies from actinolitic-hornblende to actinolite (names after

Leake, 1978).

epidote (czoV)

Clinozoisite V and czoIV amount to up to 5 vol.% of the rocks and have the same composition.

Clinozoisite V occurs as large up to 100 µm anhedral grains in the mineral aggregates replacing

garnet.

chlorite (chl)

Chlorite amounts to up to 10 vol.% in group 4 eclogites. Composition, distribution and textural

position are the same as in group 3 eclogites. The difference between group 3 and 4 eclogites lies

mainly in the larger amount of chl that cannot be attributed to grt or pg in group 4 eclogites.

titanite (ttn)

Titanite amounts to nearly 4 vol.% of group 4 eclogites. It occurs as anhedral grains of up to

100 µm in size, often with some rt or ilm in its core. It also occurs as euhedral (up to cm-sized)

grains in the host rock of some ttn-bearing quartz veins. Its composition (Table C17 in app. C) is

Ca(Ti0.95

Al0.05

)[SiO4](O,OH,F).


In the group 4 eclogites the mineral assemblage is ab, green amp, chl, czoV, and ttn. Green amp,

chl, and CzoV still have large variations in their compositions, partly due to formation at different

27

Table 6

Mineral compositions of the minerals used by Evans (1990) to construct his petrogenetic grid and thecomposition of these minerals in the metabasic rocks at Lago di Cignana.

textural sites and partly inherited from earlier replacement stages. However, compared to group 3

eclogites the amount of these two minerals with intermediate compositions has increased. This

indicates that the size of the local equilibrium domains has increased, but is still below the size of

a thin section. In the greenschists, the size of the equilibrium domains is larger than the thin section.

PT-estimates

No reliable geothermobarometers exist for this low temperature mineral assemblage (e.g. Essenne,

1989; Evans, 1990) and one has to rely on petrogenetic grids to obtain pressure and temperature

estimates for these rocks. In the petrogenetic grid of Evans (1990), for a similar bulk rock composition

as the Lago di Cignana metabasic rocks (Table 6), the assemblage actinolitic amphibole, albite,

epidote, chlorite and quartz is stable at pressures below 0.7 GPa, relatively independant of

temperature. A reliable temperature for this replacement stage cannot be obtained with the Holland

& Blundy (1994) plagioclase amphibole thermometer, because even more amphiboles than in group 3

eclogites have compositions with Si > 7.7 pfu and are outside the compositional limit of the thermo-

meter (Holland & Blundy, 1994). These amphiboles, however, indicate formation at temperatutes

below 475 °C. Consequently, the mineral paragenesis of group 4 eclogites and the greenschists

probably formed at temperatures below 475 °C and pressures below 0.7 GPa.

3.2 Structures in the eclogites

The only primary structures discernible in the metabasic rocks from Lago di Cignana are deformed

pillows, which have been described from many locations within the Zermatt Saas zone (e.g., Bearth,

1959; Oberhänsli, 1982). Where preserved, they consist of omp-rich cores grading into gln-rich

rims. The interstices between individual pillows are filled by a gln-rich matrix with qtz and carbonate.

In most cases, however, the group 1 eclogites reveal a compositional banding of alternating gln-

and omp-rich layers. This banding, presumably, originated from extreme flattening of pillows. This

interpretation is supported by the observation of structures resembling isoclinal fold hinges in gln-

rich layers, always with gln poorer eclogite in the core, as well as by the discontinuous compositional

banding and the gradual changes in gln-content.

28

Figure 12

Microstructure of a group 1 eclogite: Grt poikiloblast in a matrix of omp, gln with rims of blue-green amp,rt with ttn rim, czo and pg. Strain shadows at grt filled with omp. The foliation S

1e, defined by the shape

preferred orientation of omp, gln, pg and czo aggregates lies horizontal. Shear bands S2e

(indicated bydashed lines) follow the boundaries of the strain shadows. Note the irregular, patchy distribution of blue-green amp-ab symplectites on intergranular fractures and along omp high-angle grain boundaries and ampovergrowths on grt. The thin dashed line in grt indicates the change of the trend in compositional zoning(Fig. 6). Grt contains inclusions of omp, rt and box-shaped czo-pg ± ttn pseudomorphs after lawsonite.

The compositional banding, together with a shape preferred orientation of omp, gln, pg, and

elongated (clino-)zoisite aggregates (Fig. 12) defines the foliation (S1e

) that strikes approximately

NE and dips with an angle between 20 and 50° towards the NW (Fig. 13). The orientation of S1e

varies between different outcrops, but the spread usually overlaps. On this foliation, a stretching

lineation (L1e

) is defined by the long axes of gln crystals and elongated aggregates of (clino-)zoisite.

The stretching lineation plunges with around 15° to the WNW (Fig. 13). The foliation S1e

flows

around garnets with symmetric strain shadows filled with coarse-grained (400 µm) omp (Fig. 12).

This shows that grt had grown before deformation D1e

. The finer grained (40 µm) matrix omp has

serrated grain boundaries. This indicates that omp deformed plastically by a combination of

dislocation creep and dynamic recrystallisation by grain boundary migration (Buatier et al., 1991;

Godard & van Roermund, 1995). In rocks completely transformed to a lower grade paragenesis, the

compositional banding is no longer discernible. The foliation S1e

is, however, preserved due to

pseudomorphic replacement of the UHPM minerals by lower PT-replacement products (Fig. 14).

The czo aggregates after zoi and pg, and the symplectites of ab and blue-green amp after omp and

gln, preserve the shape of the precursor mineral grains and, in this way, the foliation.

29

Figure 13

Orientation of structural elements in eclogites, depicted in stereographic projections (lower hemisphere,equal area). Left: foliation S

1e, lineation L

1e and shearbands S

2e. Center: π-pole construction of D

3e open

folds. Right: orientation of veins.

Locally, S1e

is crosscut by extensional shearbands (e.c.c.´s = extensional crenulation cleavage,

S2e

) (Figs. 12, 13). The distribution of S2e

is heterogeneous. Zones with closely spaced shearbands

alternate with zones were they are rare. Orientation of S2e

varies between the outcrops, as does the

foliation S1e

. Usually, two sets of shearbands form a conjugate system with one of the orientations

dominating in one outcrop. Shearbands nucleated at garnets following the S1e

strainshadow interface

and developed by coalescence of these domains. S2e

is defined by a shape preferred orientation of

omp. The coarser grainsize (up to 400 µm) of omp along S2e

compared to the matrix, indicates that

S2e

had formed before transformation of the eclogite to a lower grade mineral paragenesis had

started. There is no systematic difference in compositions between matrix omp and coarse grains in

S2e

. Furthermore, a quartz pseudomorph after coesite has been found in one of the coarse omphacites.

All these evidences suggest that S2e

(e.c.c.) formed under UHP metamorphic conditions. In eclogites

transformed to lower grade paragenesis, S2e

was preserved, because symplectites of ab and blue-

green amp preserve the shape of precursor omp grains. The frequently observed concentration of

minerals formed during lower PT-replacement along S2e

is attributed to later fluid infiltration focused

along these discontinuities. Fluid infiltration is also suggested by the relative abundance of quartz

and calcite along S2e

compared to the host rocks.

Later localisation of deformation in the eclogites is revealed by several generations of veins of

various kind and scale and by other structures. Veins will be presented first, because they can be

used as a reference frame for later deformation stages. The microstructures, fabrics, and fluid

inclusions data from veins will be presented in chapter 5. Veins in the eclogites can be classified

into four groups (Fig. 15).

30

Figure 14

Histograms showing the abundance of measured angles between foliation and shortest dimension of mineralsor mineral aggregates for eclogites with different amounts of lower PT-replacement products. Mineralaggregates that formed at the expense of UHP minerals approximately preserve the shape preferred orientationof this mineral and in this way the foliation. In group 3 and 4 eclogites, growth of a amphibole at the expenseof symplectitic amphibole partly destroys this pattern.

Type Ie veins are orientated sub-parallel to the foliation S

1e (Fig. 13, 15). They exhibit low aspect

ratios (< 5) and the opposing flanks do not fit. The vein mineralisation is composed of czo or

qtz often accompanied by minor amounts of omp, gln, ap, and rt, or by minor amounts of ttn,

and czo. Quartz in these veins is completely recrystallised. Other minerals are usually subhedral,

without any obvious lattice or shape preferred orientation. Where abundant, czo forms fibers

perpendicular to the vein flanks. The least transformed host rocks of type Ie veins are the

group 1 eclogites.

Type IIe veins are orientated sub-parallel to the foliation S

1e or sub-parallel to the shearband

foliation S2e

(Fig. 13, 15). Their aspect ratio ranges up to 10. There is no fit between the

31

Figure 15

Schematic diagram (not to scale) depicting orientation, crosscutting relations and aspect ratios of the differentvein types and their relation to orientation of foliation S1

e and shearbands S2

e as seen on a horizontal plane.

Chronological relations between type Ie and type II

e veins could not be deduced. Strike of the foliation is NE

with 20-50° dip to the NW. The trace of UHPM extensional shearbands cuts the foliation at a low angle.Late shear zones possibly synchronous with type IV

e veins are not shown.

opposing flanks. The vein mineralogy is qtz, often associated with czo or ttn. The qtz is partly

to completely recrystallised. Other minerals present in these veins occur as subhedral grains

without shape preferred orientation. The least transformed host rocks of type IIe veins are the

group 2 eclogites.

Type IIIe veins are orientated at a higher angle (> 30°) to the foliation S

1e and the shearbands S

2e

(Fig. 13, 15). They have aspect ratios up to 40. Usually, there is no fit between the opposing

flanks. Their mineralogy is qtz with green amp, with ttn or with czo. The qtz is partly to

completely recrystallised. Other minerals present in these veins occur as subhedral grains,

without obvious shape preferred orientation. The host rocks of type IIIe veins are mainly the

group 3 and 4 eclogites.

Type IVe veins are also orientated at a high angle to foliation S

1e and shearbands S

2e (Fig. 13, 15).

These veins have a high (> 30) aspect ratio and the opposing flanks fit. Their mineralogy is

ab, often with green amp and rarely epidote. The primary vein filling structure is preserved,

32

Figure 16

Schematic sketch of mesoscopic structural relations between eclogites, greenschists and metasedimentaryrocks at Lago di Cignana. Late shearzones in eclogite (D

4e1, D

4e2) and veins in eclogites and metasedimentary

rocks are not shown.

with fibrous ab, amp and epidote, oriented perpendicular to the vein flank. Crosscutting

relations between ab veins, indicate that at least three generations of ab veins exist. The host

rock of type IVe ab veins are the group 4 transformed eclogites.

Locally, foliation S1e

is folded on an m to 10 m scale, clearly discernible on stereographic

projections of the foliation poles (Fig. 13). On the outcrop scale, open folds with a corresponding

orientation (E-W trending fold axes) and a wavelength in the dm- to cm-range are observed. Initial

stages of an axial plane crenulation cleavage (S3e

) are developed in places. The fold limbs of these

microfolds are enriched in amphibole when compared to the fold hinges, indicating that dissolution

precipitation creep was involved. A type Ie or II

e qtz vein has also been folded. The folding of

foliation S1e

in some group 4 transformed eclogites, suggest that deformation D3e

took place at

T < 475 °C and P < 0.7 GPa.

Late shear zones (D4e1

) occur in an eclogitic lens within the metasedimentary rocks. The

continuation of the shear zones into the metasedimentary rocks is not exposed. The shearzones

strike between E-W and NE-SW and dip with 60° NNW. They acted as normal faults with a dextral

strike slip component. Each zone is 30 to 40 cm wide; with the spacing in between ranging from 1.5

to 3 m. The displacement across each individual shear zone is in the order of a few cm as indicated

by displaced early albite veins. These shearzones are crosscut by late ab veins.

Another shear zone (D4e2

) occurs in a qtz-ab vein in eclogite. Deformation concentrated in the

10-15 cm wide vein, with the wall rock of the vein, consisting of group 4 transformed eclogite,

33

remaining undeformed. The vein strikes NNE-SSW and dips with 60° W. The exposed length is

approx. 10 m; the magnitude of displacement is unknown. The sheared vein is crosscut by late ab

veins.

3.3 Structures in the greenschists

More intensive deformation led to the transformation of the pseudomorphically replaced group 4

eclogite into a true greenschist. Therefore, deformation of the greenschists must have occurred at T

< 475 °C and P < 0.7 GPa. The foliation of the greenschists (S1g

, strike NE, dip 30° NW) is defined

by alternating layers of amp or ab and by a shape preferred orientation of green amp (grainsize ca.

100 µm) and epidote, and developed out of S3e

. The main foliation is isoclinally folded (D2g

), with

transposition of S1g

to S2g

, but without development of a new foliation in the fold hinges. Amphibole

has partly recrystallised in the fold hinges. Locally, this foliation (S1g

/S2g

) is folded on an m- to cm-

scale around E-W trending fold axes with a steep axial plane striking approximately E-W (D3g

).

Furthermore, open folds with vertical N-S (D4g

) and E-W (D5g

) striking axial planes occur. The

orientation of the folds in the greenschists is similar to the orientation of the folds in the

metasedimentary rocks (Fig. 16, 17). The greenschists are devoid of veins.

34

4 The record of the metasedimentary rocks

In this chapter the petrologic and structural records of the metasedimentary rocks will be presented.

The record preserved in the veins of the metasedimentary rocks is presented in chapter 5.

4.1 Petrology of the metasedimentary rocks

The petrology of the metasedimentary rocks is a summary of the results of Reinecke (1991;

1995; 1998). The metasedimentary rocks are mainly garnet-phengite-quartz-schists, with variable

amounts of dolomite, calcite, paragonite, and epidote. Subordinately, garnet-clinopyroxene-quartzites

and piemontite-phengite-quartz-schists occur. The bulk rock composition is very heterogeneous

and often changes on a cm-scale. Some samples show up to three stages of garnet growth, associated

with varied low-variance inclusion assemblages as well as compositionally zoned phases (e.g.,

phengite, dolomite, calcite) and distinct reaction textures in the matrix. These rocks provide ample

information for the reconstruction of their PT-path. Combining results derived by methods of absolute

(geo-Calc-Software: Brown et al., 1988, database of Berman, 1988) and relative thermobarometry

(Spear, 1988; Spear & Menard, 1989; Spear, 1993) from three different bulk rock compositions,

Reinecke (1995; 1998) has produced a well constrained PT-path of the metasedimentary rocks at

Lago di Cignana. The principal results are given below:

Maximum pressures of about 2.8-3.0 GPa were attained at about 600 °C. The thermal peak was

reached at 30-45 °C higher temperatures and 0.2-0.3 GPa lower pressures.

Early denudation to approx. 2.3 GPa, into the stability field of quartz, was accompanied by a

significant (about 50 °C) temperature decrease.

Decompression from 1.7-1.9 GPa to 1.1-1.2 GPa was almost isothermal (at 500-550 °C).

Further decompression from about 1.1 GPa to 0.6 GPa was accompanied by a temperature decrease

from 550 to 450 °C.

A late greenschist facies overprint occurred at 350-420 °C and 0.2-0.5 GPa.

4.2 Structures in the metasedimentary rocks

The compositional banding in the metasedimentary rocks is interpreted as bedding. Sub-parallel

to this banding a foliation is developed. Isoclinal folds in compositional bands and foliation prove

that the dominant schistosity is at least the second foliation (S2s

, strike NE, dip 20° SE, Fig. 17).

The foliation is defined by alternating layers rich in quartz and mica, and by the shape preferred

orientation of phengite, clinozoisite/epidote, and albite-amphibole symplectites. The stretching

lineation (L2s, trend WNW, plunge subhorizontal, Fig. 17) is defined by the shape preferred orientation

of clinozoisite/epidote. Boudins of metabasic and quartzitic rocks in a matrix of mica rich rocks are

observed in this foliation. The width of the boudins is up to 30 cm and their length up to 40 cm. The

boudin necks are filled with quartz and clinozoisite. The quartzitic boudins are slightly rotated

along N-S striking, 20° E dipping shearzones. The asymmetric strain shadows at the eclogitic boudins

suggest non coaxial deformation and top to the N displacement (Photo 8). Because S2s

always flows

35

around garnets, these must have been mechanically effective during formation of foliation S2s

.

Reinecke (1995) calculated the PT-path of the metasedimentary rocks from profiles of zoned garnets.

Therefore, S2s

must have formed after the last garnet growth at T < 450 °C and P < 0.6 GPa (Reinecke,

1995). In some rock types, the foliation S2s

is partly defined by the shape preferred orientation of

fine grained aggregates of tremolite + microcline + albite + hematite ± jadeite poor aegerineaugite,

that replace UHPM aegerineaugite with jd26-37

(Reinecke, 1995). These fine grained aggregates are

undeformed, indicating that the replacement occurred after formation of the foliation. Therefore,

S2s

must have formed before the late greenschist reequilibration at 350-420 °C and 0.2-0.5 GPa

inferred by Reinecke (1995) from these aggregates.

Locally, the foliation S2s

is folded on a mm- to 10-m scale (figure 19). A first generation of ap-

proximately N-verging folds (D3s

) developed an axial plane crenulation cleavage (S3s

strike E-W,

dip vertical) in mica rich layers. Foliation S3s

is defined by a shape preferred orientation of mica and

clinozoisite. Foliation S2s

and S3s

are locally folded on a cm- to m-scale. The relative timing of for-

mation of the later generations of open folds (D4s

and D5s

) is unclear, because an axial plane cleavage

has not developed. Axial planes of D4s

and D5s

folds strike approximately NE-SW and N-S,

respectively, and are almost vertical. Distinction between small scale D3s

and D4s or 5s

folds is only

possible, when both generations occur in close contact and can be correlated with m-scale folds.

These deformation phases could not be correlated with petrologic observations.

In the metasedimentary rocks, veins can be classified into four groups using their relation to

foliations S2s

and S3s

, vein mineralogy and microstructure. The deformation microstructures and

fabrics of veins will be presented in chapter 5.

Figure 17

Orientation of structural elements in the metasedimentary rocks, depicted in stereographic projections (lowerhemisphere, equal area). Left: Poles of foliation S

2s and stretching lineation L

2s, Right: Poles of foliation S

3s

and axial planes to smal scale D4s or 5s

folds

36

Type Is veins are oriented sub-parallel to the foliation S

2s. They often form lenses in the foliation

that are the hinges of (refolded) isoclinal folds. The veins are mineralised with quartz, often

associated with garnet and white mica. In some veins, garnet is the main vein filling mineral.

Quartz in the veins is completely recrystallised. Garnet and white mica are euhedral and

white mica has a shape preferred orientation parallel to the foliation outside the vein. In one

garnet from these veins, an inclusion of coesite was unequivocally identified. This suggests

that at least some of the earliest veins were formed at UHPM conditions or prior to UHPM

and recrystallised during UHPM.

Type IIs veins are oriented at an angle (> 10°) to foliation S

2s and are sometimes folded by D

3s.

Aspect ratios of unfolded veins are high (> 20) and opposing vein flanks fit. These veins are

mineralised with quartz and clinozoisite. Quartz in those veins is partly recrystallised. Clino-

zoisite grains are subhedral and often broken.

Type IIIsveins crosscut S

2s and (where present) S

3s. These veins have high aspect ratios (> 30)

and opposing flanks fit. They are mineralised with quartz and clinozoisite and/or green

amphibole. A vein filling structure is preserved with large (cm-sized) quartz grains, that often

Photo 8

A lens of high viscous eclogite in a matrix of lowviscous metasedimentary rocks. The assymmetricstructure suggests a high degree of non coaxialdeformation. N is up, length of eclogitic lens is ca.0.5 m.

Photo 9

Dust trails in vein albite, define an older growthstructure. Long side of photograph is 7 mm.

37

enclose mm-sized amphibole needles. When clinozoisite is present, it forms cm-sized, sub-

hedral grains.

Type IVs veins are oriented at an angle to S

2s and (where present) S

3s. These veins have high

aspect ratio (> 30) and opposing flanks fit. They are mineralised with albite. A vein filling

structure is preserved, with mm-sized subhedral albite grains, that extend from the vein flanks

to the vein centre. The centre of the vein is often an open cavity. Fine dust trails in the albite

grains trace the outlines of older minerals (Photo 9).

38

5 Quartz veins (microstructures, fabrics and fluid inclusions)

Microstructure and fabrics of the veins give information about the stress and strain history of the

host rock after vein formation and are presented first. Fluid inclusions in the veins can give

thermobarometric information (e.g., Sheperd et al., 1985) and are presented at the end of the chapter.

5.1 Microstructures of vein quartz

In most quartz veins in the eclogites and the metasedimentary rocks, the primary microstructure

is destroyed due to subsequent deformation by dislocation creep, that caused partial to complete

recrystallisation. Locally, relic grains with a diameter of up to several millimetres are preserved in

the veins; they are composed of subgrains (Photo 10).

Most quartz veins in eclogite and type Is veins in the metasedimentary rocks have a recrystallised

grain size ranging from 70 to 125 µm. The presence of other minerals, especially of white mica in

some veins in the metasedimentary rocks, locally influenced size and shape of the recrystallised

grains. Usually, the recrystallised grains are elongated and have a slight shape preferred orientation.

Photo 11

Microstructure of quartz in a deformed type IIe vein.

The straight grain boundaris and the 120° angle atthe grain edges indicate that recrystallisation wasfollowed by grain growth under low differentialstress. Crossed polars, long side of the photograph is1.4 mm.

Photo 10

Microstructure of a type IIe quartz vein close to a

late shearzone. The polygonisation and subgrainformation of the large grain and the recrystallisationat its rim are inferred to be due to an earlierdeformation stage. Sutured grain boundaries andundulatory extinction in the recrystallised grains aredue to an overprint at lower temperatures. Crossedpolars, long side of the photograph is 7 mm.

39

The grain boundaries are straight and meet with angles near 120° at grain edges (foam structure,

Photo 11), indicating that the deformation was followed by normal grain growth under low differential

stress.

This foam microstructure has been overprinted near the later shear zones in the eclogites (D4e

)

and in type Is and II

s veins in the metasedimentary rocks folded during D

3s(Photos 10, 12, 13).

Deformation by dislocation creep under lower temperatures and higher differential stress is reflected

by undulatory extinction and irregularly serrated high angle grain boundaries and small recrystallised

grains. The recrystallised grain size is around 40 µm in shearzone 1 (Photo 12) and the folded veins

in the metasedimentary rocks and around 10 µm in shearzone 2 (Photo 13).

5.2 Paleopiezometry

In the material science, it was noted early that the differential stress during steady state creep of

metals and alloys could be related to the recrystallised grain size (e.g., Bird et al., 1969; Luton &

Sellars, 1969; Glovers & Sellars, 1973). This relation was later applied to geological materials,

mainly quartz and olivine (e.g., Mercier et al., 1977; Twiss, 1977; 1986). Derby & Ashby (1987)

and Derby (1991) propose that the steady state grain size at constant differential stress results from

Photo 13

Core and mantle structure in a late intensivelydeformed quartz vein (D

4e2). Crossed polars, long

side of the photograph is 7 mm.

Photo 12

Microstructure of a quartz vein in a small shearzone(D

4e1) in an eclogite lens. Note the bimodal grain size

distribution. In the upper right of the picture aglaucophane with small quartz inclusions occurs.Crossed polars, long side of the photograph is 7 mm.

40

a balance between the speed of recrystallisation and the rate of nucleation of new grains. This

theory explains the general relation between differential stress and recrystallised grain size:

d/b = Kn ((σ

1 - σ

3)/ µ)-n,

with d grainsize, b burgers vector, (σ1 - σ

3) differential stress, µ shear modulus and K

n and n constants.

Twiss (1977), derived values for these constants theoretically. Other authors determined these

constants by fitting the general relation to experimental data. This can be done by inserting b and µ

values for one mineral (e.g., quartz) in the formula and fitting this formula to data from experiments

on this mineral (e.g., Mercier et al., 1977; Koch, 1983; Ord & Christie, 1984), or by normalising the

experimental data from several minerals and metals (d/b and (σ1 -σ

3)/µ) and fitting the normalised

formula to the data (e.g., Skrotzki, 1992). The various calibrations of the recrystallised grainsize

paleopiezometer for quartz (e.g., Twiss, 1977; Mercier et al., 1977; Koch, 1983; Ord & Christie,

1984; Skrotzki, 1992), yield highly differing results (Fig. 18). The calibrations based on experiments,

yield for a given grainsize the highest differential stresses. These experiments were performed in a

Griggs-Blacic solid-medium deformation apparatus (Griggs, 1967; Blacic, 1972), with either talc,

pyrhophyllite, AlSiMag or copper as confining medium (e.g., Koch et al., 1989). Green & Borch

(1989; 1990) showed that the strength of the materials used as confining medium could result in a

large overestimate of the flow stress and recommended the use of salt as confining medium to

Figure 18

Several calibrations of the dynamically recrystallised grain size paleopiezometer for quartz, from Twiss(1977), Mercier et al. (1977), Koch (1983), Ord & Christie (1984), Skrotzki (1992). The barred line representsthe range of recrystallised grain sizes found in a completely recrystallised sample deformed at ca. 200 MPaby Gleason et al. (1993).

41

minimise this problem. The experiments of Gleason et al. (1993) using salts as confining medium,

provide independent data to check the different calibrations. These authors report for one sample

with a pre-deformation grain size of about 50 µm, a recrystallised grain size between 5 and 10 µm

after 75 % shortening. The differential stress in this experiment was ca. 200 MPa (Gleason et al.,

1993). This data point corresponds very well with the calibration of Twiss (1977) (Fig. 18). Therefore,

the Twiss (1977) calibration of the recrystallised grainsize paleopiezometer will be used in this

study.

In veins in eclogites and metasedimentary rocks, where the recrystallised grains show indications

of normal grain growth, the recrystallised grain size ranges between 70 and 125 µm. The micro-

structure changed after deformation and does not reflect the differential stresses during deformation

any longer. However, the preservation of a shape preferred orientation, suggests that the increase in

grainsize was only moderate. The paleopiezometer of Twiss (1977) indicates minimal differential

stresses for this deformation of 25 to 35 MPa. In the group IIs veins in the metasedimentary rocks

and the veins deformed during D4e1

, quartz is only partly recrystallised with grain sizes ranging

from 20 to 40 µm. In this case, the paleopiezometer should not be used, because it is not certain that

a steady state microstructure is reached. The recrystallised grain sizes of ca. 10 µm of completely

recrystallised veins deformed during D4e2

, points to differential stresses of ca. 125 MPa.

5.3 C-axis fabrics in quartz veins

For all recrystallised quartz veins, the c-axis fabrics were measured with standard universal

stage techniques (e.g., Turner & Weiss, 1963).

5.3.1 Eclogites

The development of foliation and lineation in the eclogitic host rock predated formation and

deformation of the quartz veins. Thus, these structural elements cannot be used as kinematic

framework. Therefore, the textures are referred to the finite strain axes, assumed to be parallel and

normal to the foliation and lineation defined by the shape preferred orientation of the recrystallised

grains (Price, 1985). The measured c-axis fabrics range from point maxima, to single girdles, and

weakly developed type I cross girdles (Lister, 1977), oriented at a high angle to this foliation (Fig. 19).

Owing to the isolated position of the veinlets in essentially undeformed eclogites, accumulation of

a large strain is precluded. Hence, the lattice preferred orientation developed during deformation is

probably influenced by the orientation of the pre-existing grains. In fact, point maxima are

characteristic for veins with mm-sized relic grains and better defined c-axis girdles occur in

completely recrystallised veins. As such, the variation in lattice preferred orientation seemingly

reflects the intensity of deformation.

For a vein deformed in shear zone 1 (D4e1

) the shear zone boundaries are taken as the kinematic

framework. The c-axis fabric is diffuse (Fig. 19, Bk 119). Taking into account the small amount of

displacement along this shearzone and the bimodal recrystallised grainsize distribution, the diffuse

c-axis fabric probably reflects the overprinting of two stages of low finite strain deformation.

42

For the veins deformed during D4e2

, the shear zone boundaries are not found and the textures are

referred to the finite strain axes, assumed to be parallel and normal to the foliation and lineation

Figure 19

Lattice preferred orientation of quartz (c-axes) in selected veins in eclogite, that underwent grain growthunder low differential stress after deformation (Bk 4,5,8,20,118) and a vein that deformed during D

4e1 (Bk 119).

Data are presented as scatter plots and contour plots. The orientation with respect to mesoscopic structuresis for all veins only approximate. Bk 5 and Bk 8 are type I

e veins, Bk 4 and Bk 20 are type II

e veins and Bk

118 is a type IIIe vein. See text for discussion.

Z

X

Z

X

��

��

Z

X

Z

X

��

��

��

��

Z

X

Z

X

Z

X

Z

X

��

��

Z

X

Z

X

��

��

��

��

Z

Z

X

43

defined by the shape preferred orientation of the recrystallised grains (Price, 1985). The c-axis

fabrics for these veins are single girdles, tending towards type I crossed girdles (Fig. 20).

5.3.2 Metasedimentary rocks

For type Is veins the foliation S

2s and the stretching lineation were taken as kinematic framework.

The c-axis fabrics of the type Is veins (Fig. 21) are double point maxima with one maximum approxi-

mately normal to X and Z and the other maximum at a high angle to X and Y. These could be inter-

preted as single girdles at a high angle to the foliation. Sample Bk 77 has large variations in c-axis

orientations. This sample is from an isoclinally folded quartz vein that was refolded by D3s

. The

large spread in c-axes reflects an overprinting of an earlier fabric by a stage of low finite strain

deformation.

For type IIs veins the foliation S

3s and the direction normal to the fold axis were taken as kinematic

framework, where S3s

had developed. In the other cases (Bk 46, Bk 99) the textures are referred to

the finite strain axes that are assumed to be parallel and normal to the foliation and lineation defined

by the shape preferred orientation of the recrystallised grains (Price, 1985). The c-axis fabrics of the

type IIs veins (Fig. 22) are broad point maxima tending to weakly developed single girdles. The

broad point maxima probably reflect the influence of the orientation of the large pre-existing grains

on the developing lattice preferred orientation. It seems, that D3s

deformation of the veins was not

intense enough to produce a complete new c-axis fabric. This is supported by sample Bk 77, where

the earlier c-axis fabric is only slightly modified by later D3s

deformation.

Figure 20

Lattice preferred orientation of quartz (c-axes) of veins deformed during D4e2

. Data are presented as scatterplots and contour plots. The orientation with respect to mesoscopic structures is for all veins only approximate.

Z

X

Z

X

Bk 131A N = 250

Z

X

Z

X

��

��

Z

X

Z

X

Bk 130 N = 250

44

5.3.3 Summary

The c-axis fabrics for most veins in eclogites and metasedimentary rocks are not well enough

developed to estimate strain ratios or sense of shear from these fabrics (e.g., Price, 1985). Only

veins deformed in shear zone (D4e2

) have well-developed c-axis fabrics that suggests non coaxial

deformation in this shearzone with a dextral sense of shear (Price, 1985). The c-axis girdles

approximately normal to the foliation, indicate that <a> glide on various lattice planes (e.g., Schmid

& Casey, 1986) was the predominant deformation mechanism. The predominance of <a> glide on

various lattice planes, suggests deformation at relatively low temperatures (Hobbs, 1985).

5.4 Fluid inclusions in vein quartz

Fluid inclusions are samples of a fluid phase that may be present during a certain moment in the

history of the rock. They are the only direct evidence for the presence of a fluid phase and the only

possibility to physically analyse the composition of this fluid phase (e.g., Roedder, 1984). In this

study, it is more important that under certain conditions thermobarometric data can be obtained

from these inclusions (e.g., Roedder, 1984; Shepherd et al., 1985). Fluid inclusions can be used as

thermobarometer, when their composition and density can be determined and when P(ressure)-

V(olume)-T(emperature)-data for this composition are available. If the composition and volume of

the inclusion did not change after formation, PT-conditions for the formation of the fluid inclusion

can be inferred (e.g., Roedder, 1984).

Figure 21

Lattice preferred orientation of quartz (c-axes) in veins subparallel to foliation S2s

. Data are presented asscatter plots and contour plots.

��

��

X

X

Z

Z

��

��

��

��

X

X

X

X

Z

Z

Z

Z

45

To interpret these PT-data the origin of the fluid inclusion must be known. Usually, a distinction

between primary inclusions that formed during the growth of the host mineral and secondary inclu-

sions that formed after the growth of the host mineral is made (Roedder, 1972).

Fluid inclusions were studied in partly to completely recrystallised type Ie and II

e quartz veins.

The arrangement of the high angle grain boundaries of the recrystallised grains in these samples

suggests late grain growth under low differential stress. In the recrystallised and relic grains four

types of fluid inclusions are recognised:

1. Single fluid inclusions in the recrystallised grains are considered to have formed during

recrystallisation (e.g., Wilkins & Barkas, 1978).

2. Fluid inclusions arranged along irregular planes in the recrystallised grains (Photo 14) are

interpreted as relics of a grain boundary porosity in an originally finer grained microstructure

and thus must have formed during recrystallisation (e.g., Wilkins & Barkas, 1978).

3. Fluid inclusions arranged along planes delineating subgrainboundaries in the relic grains are

considered to have formed during polygonisation (e.g., Wilkins & Barkas, 1978).

4. Fluid inclusions arranged along planes that crosscut grain boundaries are interpreted as healed

microcracks (e.g., Sprunt & Nur, 1979) and considered to have formed after recrystallisation.

This allows subdivision of the fluid inclusions in two main groups:

Early inclusions of the type 1, 2, and 3 that formed during deformation and recrystallisation of

the original vein filling material and are secondary inclusions after Roedder (1972) with

Figure 22

Lattice preferred orientation of quartz (c-axes) in veins deformed in D3s

. Data are presented as scatter plotsand contour plots.

��

��

��

��

��

��

x x x

x x x

z z z

z z z

46

respect to the relic grains. These inclusions, however, formed during the formation of the

recrystallised grains and are, therefore, primary inclusion for the recrystallised grains.

Late inclusions of type 4, that formed after formation of the recrystallised grains are true secondary

inclusions after Roedder (1972).

The composition of fluid inclusions is determined through observation of phase transitions at

low temperatures. Most fluid inclusions at Lago di Cignana can be described in the relative simple

system H2O-salt and only the phase transformations, that are observed upon heating of a frozen

inclusion in this system, will be described.

The first phase transition upon heating after cooling, which is only sometimes observed, is the

onset of melting (temperature of eutectic between solid and liquid phase). This temperature indicates

which cations might be dissolved in the fluid phase (e.g., Hollister & Crawford, 1981). Because the

amount of first melt is very small, the temperature at which this transition is observed will always

be higher than the real temperature of eutectic (Küster, 1994).

The next phase transition that occurs in this system, is the melting of the last ice. From the

freezing point depression the salinity of the fluid can be calculated (Roedder, 1984).

The density of a fluid inclusion of known composition is determined by measuring the homo-

genisation temperature. Homogenisation occurs when the vapour bubble in the inclusion disappears.

In the fluid inclusions from Lago di Cignana homogenisation was always in the fluid phase (inclusions

have a supercritical density); upon heating the vapour bubble becomes smaller and finally disappears

(Roedder, 1984). With these observations and if P-V-T-data for these compositions are known, the

positions of isochors in the PT-field can be determined (e.g., Haas, 1976; Potter & Brown, 1977).

Photo 14

Fluid inclusions arranged along irregular planes in a recrystallised grain, are interpreted as relics of a grainboundary porosity in an originally fine grained structure. In the lower left corner of the photograph a trail ofsecondary inclusions occurs. Plane polarised light, length of scale bar 125µm.

47

The temperatures determined for all observed phase transitions must be corrected according to

the calibration curve for the heating-freezing stage used (Roedder, 1984). Compositions and densities

can then be calculated with the program FLINCOR 1.2.1. using the corrected Tm H

2O and T

hom H

2O.

The position of the isochores in the PT-field was calculated with the equation of state of Brown &

Lamb (1989) in the system H2O-NaCl. Other equations of state for this system (e.g., Haas, 1976;

Potter & Brown, 1977; Zhang & Frantz, 1987) give similar results. Graphical representation of the

isochores in a PT-diagram was facilitated with the program FCP of Dr. Röller.

A problem is that the composition (salinity) of the inclusion is inferred from the freezing point

depression. The depression depends on the amount and on the kind of anions and cations in the

solution. The eutectic temperature suggests which cations might be solved. It gives, however, no

indication of the amounts of these cations in the solution. Furthermore, P-V-T-data are not known

for more complex salts solved in a fluid phase. Therefore, the salinity of the fluid is approximated

in wt.% NaCl-equivalent, because Na+ and Cl- are usually the dominant ions in the fluid phase

(Roedder, 1962). Because the eutectic temperature of the H2O-NaCl system is -20.8 °C, fluid

inclusions with melting temperatures below this temperature cannot be processed. Melting

temperatures at Lago di Cignana were, however, all above this temperature.

5.4.1 Compositions and densities of the fluid inclusions

Fluid inclusions were analysed in three quartz veins that are partly to completely recrystallised.

Bk 20 is a type IIe quartz clinozoisite vein in a group 3 eclogite. Bk 100 is a type I

e quartz omphacite

segregation in a group 1 eclogite. Bk 101 is a type IIe quartz vein in a group 3 eclogite that is part of

a swarm of veins parallel to the foliation in eclogite, that occur within 0.5 m from the contact

between eclogite and metasedimentary rock.

All measured inclusions in these quartz veins were at room temperature 2-phased and contained

an aqueous fluid of low salinity. At room temperature single phase inclusions were not measured,

while even at very low temperatures, usually, no phase transformations were observed. These

inclusions contain a low density vapour or a high density fluid phase. The absence of a vapour

bubble in a fluid phase could also be due to metastable behaviour of the inclusion (Roedder, 1967).

Metastable behaviour was observed in several inclusions that were initially 2-phased, but were

single phase after one or more cooling and heating cycles.

For the early inclusions, observed temperatures of eutectic range between -30 and -25 °C, indi-

cating the presence of other cations besides Na+ in the solution (Hollister & Crawford, 1981). The

temperatures of melting range from -1 to -11 °C (between 1.6 and 15 wt.% NaCl-equivalent).

Temperatures of homogenisation (in the fluid phase) range from 80 to 190 °C, corresponding to

densities between 0.94 and 1.07 gr/cm3 (equation of state of Brown & Lamb, 1989) (Table 7, Fig. 23).

For the late inclusions, observed temperatures of eutectic are also ca. -30 °C, indicating the

presence of other cations besides Na+ in the solution (Hollister & Crawford, 1981). The temperatures

of melting range from -1 to -11 °C (between 1.6 and 15 wt.% NaCl-equivalent). Temperatures of

48

homogenisation (in the fluid phase) range from 100 to > 250 °C, corresponding to densities between

< 0.87 and 1.05 gr/cm3 (equation of state of Brown & Lamb, 1989) (Table 7, Fig.23).

The large spread in homogenisation temperatures found in sample Bk 101 can, perhaps, be

explained by necking down of larger inclusions (Lemmlein & Kliya, 1952). In this sample fluid

inclusions were observed consisting of two spheres connected by a thin tube, indicative for necking

down. Because necking down changes the density of the fluid inclusions, only the data of samples

Bk 20 and Bk 100 are interpreted. The isochores for the fluid inclusions in these samples are depicted

in figure 24.

The thermobarometric interpretation of the fluid inclusion data assumes constant volume (density)

and constant composition for the inclusion. Several studies have shown that fluid inclusions that

from geological reasoning formed at peak metamorphic conditions, have densities and compositions,

Table 7

Temperature ranges for observed phase transformations and inferred composition and densities of early andlate fluid inclusions from the investigated samples.

Figure 23

Melting temperatures against temperature of homogenisation for the fluid inclusions in the investigatedsamples differentiated for the arrangement of the fluid inclusions.

49

that suggest pressures and temperatures of formation below these conditions (e.g., Hollister et al.,

1979; Küster, 1994 on Crete; Swanenberg, 1980, in Rogaland; Kreulen, 1980 on Naxos). Therefore,

the fluid inclusions changed after formation, either their density, or their composition. Experimental

investigations on fluid inclusions in quartz have also shown that fluid inclusions can change their

density and/or their composition (e.g., Pecher, 1981; Pecher & Bouillier, 1984; Sterner & Bodnar,

1989; Bouillier et al., 1989; Bakker & Janssen, 1990; Bakker, 1994). Compositional changes in

fluid inclusions can be explained with diffusion of material out of the inclusion at relatively high

(T > 600 °C) temperatures (e.g., Bakker, 1994). A theory, that explains the density decrease observed

for fluid inclusions in quartz at lower temperatures (T > 300 °C), has been proposed by Küster

(1994) and Küster & Stöckhert (1997). They show that at the low rate of change in P and T in

metamorphic rocks, very low strain rates are sufficient for volume adaptation of the inclusions by

dislocation creep of the host quartz. Dislocation creep is driven by the differential stresses, that

develop in the host mineral around the inclusions, when cooling and decompression does not follow

the isochor of the fluid inclusion. Therefore, they suggest that as long as the host mineral behaves

ductile, fluid inclusions will change their volume. The density of the fluid inclusions reflects the

PT-conditions at which plastic stretching of the host mineral is no longer possible. Experimentally

derived flow laws for quartz (e.g., Paterson & Luan, 1990; Koch et al., 1989) suggest that for

relevant strain rates (10-15, 10-16 s-1, Küster & Stöckhert, 1997) the flow stress drastically increases

at temperatures of about 300 °C or somewhat below.

Following the model of Küster & Stöckhert (1997), the densities of the early fluid inclusions

measured in two quartz veins at Lago di Cignana suggest a pressure between 0.2 and 0.4 GPa at

temperatures around 300 °C (Fig. 24).

Figure 24

Position of the isochores (equation of state of Brown & Lamb (1989)) for the early and late fluid inclusionsfrom samples Bk 20 and Bk 100.

50

6 The exhumation record of the rocks

Metamorphic rocks are sometimes thought of as flight recorders, black boxes recovered from

the wreckage of an orogen, that tell us something of that orogens history (Haugerud & Zen, 1991).

They differ, however, from flight recorders in that the recording is not continuous and that often

parts of the recordings are erased. The record preserved in the rock, generally depends on an incom-

plete and spatially distributed response of the rock to the changing conditions. During large parts of

the exhumation history the rocks have remained essentially passive, without undergoing discernible

modification and the exhumation history is, therefore, only partly recorded.

Two general remarks can be made concerning the record found in the rocks:

1. All orientations and directions mentioned in the text are as they occur today. During later

deformations earlier structures have been rotated.

2. Uncertainties of absolute PT-estimates pertaining to some well-calibrated geothermobaro-

meters are on the order of 50 K (1 σ) and 500 MPa (Kohn & Spear, 1991a). Differences in P

and T, however, calculated with the same thermobarometer from different samples have much

smaller uncertainties, that are commonly about a few tens of Kelvin and tens of MPa (Kohn

& Spear, 1991a; 1991b; Hodges & McKenna, 1987). This means that absolute PT-conditions

mentioned in this study have uncertainties of at least 50 K and 500 MPa, whereas relative

changes in PT-conditions are relatively well constrained, but the exact positions of these

segments of the PT-path are subject to similar errors as the absolute thermobarometry.

The metabasic and the metasedimentary rocks preserved different parts of the exhumation history.

The petrological record (Fig. 25) is nearly complete in the metasedimentary rocks (e.g., Reinecke,

1998) and a similar, but more fragmentary record is found in the metabasic rocks (this study). A

comparison of the structural records shows that in the metasedimentary rocks only the last part of

this record is preserved, but that the metabasic rocks preserved the UHPM and later parts of the

record (Fig. 25). The records of both rock types will now be combined and discussed for several

intervals.

6.1 The record during UHPM and early exhumation

In the metabasic rocks deformation under UHPM conditions (Fig. 25; T 575-625 °C;

P 2.5-2.8 GPa) is indicated by the foliation (S1e

) defined by omphacite. This deformation was

heterogeneous, as evident by the variable distortion of pillow structures. The bulk rock rheology

was controlled by omp, with the other minerals essentially acting as rigid bodies. This interpretation

is supported by the irregulary distributed composition domains found in individual omp grains,

attributed to compositional reequilibration during grain boundary migration (e.g., Buatier et al.,

1991; Godard & van Roermond, 1995), that contrast with the compositional homogeneity of other

minerals and the regular zoning pattern in garnet. Differential stresses must have been high enough

to drive deformation by dislocation creep in omphacite at temperatures of about 600 °C. Extrapolation

of laboratory data on diopside (e.g., Boland & Tullis, 1986), assumming geological relevant strain

51

Figure 25

PTD-path for the exhumation of UHPM rocks of Lago di Cignana, Western Alps, Italy, modified after vander Klauw et al., (1997). The continuous segments of the PT-path were derived by Reinecke (1995; 1998)from absolute and relative thermobarometric methods applied to compositional zoning and inclusion patternsin garnet, combined with compositional information from other zoned matrix phases of the metasedimentary

52

rates (10-14–10-16 s-1), provides an upper limit of about 200-250 MPa for the differential stress to

drive steady state creep of diopside at these conditions. Preliminary results on the deformation

behaviour of jadeite (Stöckhert & Renner, 1998) suggest that at ca. 600 °C and a strain rate of

10-14 s-1, the flow stress may be as low as a few MPa. The strength of omp is probably not the same

as that of jadeite at these conditions, but possibly well below that of diopside.

The extensional shearbands (S2e

) in the metabasic rocks indicate localisation of deformation.

Quartz pseudomorphs after coesite in omp grains on these bands, suggest that S2e

formed as the

rocks were in the stability field of coesite. The shearbands are inferred to have nucleated at the

interface between strain shadows at garnets and matrix, and thus result from the contrasts in

mechanical properties of the rock forming minerals.

Subsequent to the formation of S2e

at P > 2.7 GPa and T > 575 °C, no further deformation and

mineral reactions took place in the metabasic rocks prior to the onset of the replacement of the

UHPM mineral assemblage at 1.2 GPa and 550-575 °C. Net-transfer and exchange reactions are

probably not detected, because the mineral assemblage omp + grt + rt + gln/zoi + czoI is stable over

a large range of PT-conditions and minor possible relaxation of Fe-Mg exchange between ferro-

magnesian minerals was impeded by slow rates of volume diffusion, due to the relatively low

temperatures. Veins parallel to the foliation may have formed, but cannot be distinguished from

other vein types. Along this part of the PT-path, the differential stress remained too low to allow for

notable deformation of the metabasic rocks. Any deformation during this stage must have been

localised into weak shearzones that were not observed or located in the overlying metasedimentary

rocks. The metasedimentary rocks preserved the UHPM and early exhumation PT-record, as minerals

included in garnet, as minerals in strain shadows or as zoned minerals (Reinecke, 1995; 1998). All

structures that might have formed under these conditions were either completely transposed, or

wiped out by intense later deformation and the structural record was not preserved. The structural

record in the metasedimentary rocks starts at T > 450 °C and P > 0.6 GPa.

6.2 The record between 575 and ca. 450 °C

In the metasedimentary rocks the PT-record of Reinecke (1995; 1998) shows a change from

almost isothermal decompression to pronounced cooling with decompression in this temperature

interval (Fig. 25). In the metabasic rocks, omp in contact with qtz became unstable at PT-conditions

below ca. 1.2 GPa and 575 °C and recording resumed, showing similar PT-changes as the

metasedimentary rocks.

The spatial and implied temporal relationship between the late vein types and the extent of lower

PT-replacement in the metabasic rocks (Table 8), allows the reconstruction of the trend in the

evolution of relative fluid pressures Pf and differential stress on this part of the exhumation path

(Fig. 25).

Type Ie qtz veins were formed before or during UHPM and deformed together with their metabasic

host rock, probably as coesite veins. Therefore, they give no information about the exhumation

history, apart from structures superimposed during post UHPM deformation. According to the

53

correlation with the type of lower PT-replacement, type IIe qtz veins were formed at temperatures of

about 550 to 500 °C and type IIIe qtz veins at T < 500 °C. Shape and aspect ratio of type II

e and III

e

qtz veins, and the lack of fit between the vein flanks, indicate that the host rock deformed plastically

at the time of vein formation. In contrast, the shape of most type IVe ab veins, formed at temperatures

below ca. 475 °C, indicates that the host rocks exhibited brittle behaviour at the time of vein formation.

The orientation of the veins with respect to pre-existing structures and discontinuities can be

used to place some qualitative constraints on the magnitude of differential stress (Etheridge, 1983;

Sibson, 1985). Type IIe qtz veins are oriented parallel to foliation S

1e or S

2e; these are interpreted to

represent planes of low tensile strength. Differential stress was too low to allow formation of new

cracks in other orientations. Hence, σ3 was oriented at a large angle, but not necessarily normal to

the veins. Furthermore, formation of veins in these orientations requires that Pf exceeded the normal

stress acting across these planes; hence, Pf was larger than σ

3. This limits the magnitude of the

differential stress to very low values (Jaeger & Cook, 1979). The later formation of type IIIe qtz

veins at a high angle to the pre-existing discontinuities, requires a reorientation of the principal

stress directions to prevent cracks following pre-existing discontinuities. The three generations of

type IVe ab veins, indicate that conditions favouring the formation of open cracks at a high angle to

pre-existing discontinuities, were realised several times during later deformation history.

An upper limit for the magnitude of the differential stress during formation of tensile fractures is

given by Jaeger & Cook (1979) as σ1-σ

3 < 4Te, where Te denotes the tensile strength of the rock.

For this, Etheridge (1983) proposes 10 MPa as an upper limit in unfractured rocks under metamorphic

PT-conditions. It is expected that this magnitude is drastically reduced along pre-existing discon-

tinuities. According to these considerations, the magnitude of differential stress during formation

of type IIIe and IV

e veins is limited to less than 40 MPa, and may have been significantly lower for

the formation of type IIe veins.

Table 8

Correlation between the degree of lower PT-replacement and the number of veins present in a rock volume.

54

6.3 The record between ca. 450 and 300 °C

In the metasedimentary rocks the PT-record (Reinecke, 1995; 1998) shows a slight decomp-

ression with decreasing temperature from ca. 0.6 GPa at 450 °C to 0.2-0.5 GPa at 350-420 °C

(Fig. 25). This fits well with the PT-estimate of 0.2–0.4 GPa at around 300 °C, inferred with the

method of Küster & Stöckhert (1997) from fluid inclusions in quartz veins in the metabasic rocks.

The structural record in the metabasic rocks shows localised folding of foliation S1e

in pseudo-

morphic replaced eclogite with a greenschist facies mineral assemblage at T < 475 °C and

P < 0.7 GPa. Localisation and more intense deformation led to the development of the foliated

(S1g

/S2g

) greenschists. Lenses of metabasic rocks in the metasedimentary rocks have their foliation

(S1e

, S2e

) at varying angles to foliation S2s

of the metasedimentary rocks, if they consist of (pseudo-

morphic) eclogite; the foliation (S2g

) is parallel to S2s

, if they consist of greenschists, indicating that

S2g

and S2s

formed during the same deformation event. At this stage, also the quartz veins in the

metabasic rocks and type Is veins were deformed by dislocation creep of quartz. The recrystallised

grainsize in those veins ranges between 70 and 125 µm, indicating minimal differential stresses of

25 and 35 MPa (Twiss, 1977) for this deformation. In combination with experimentally determined

“best choice 2” flow law of Paterson & Luan (1990), these differential stresses indicate for assumed

strain rates of 10-14-10-16 s-1 temperatures between 400 and 450 °C during deformation (Fig. 26).

These temperatures are in good accordance with temperatures for D2s

inferred from petrologic

observations.

The arrangement of high angle grain boundaries in the quartz veins indicates interfacial free

energy control. This microstructure can only be attained, if no driving force for grain boundary

migration is exerted by contrasting dislocation densities. Different dislocation densities are produced

during dislocation creep deformation, that at these temperatures requires only low differential stresses

(e.g., Stöckhert et al., 1997). Consequently, the magnitude of differential stress must have been low

subsequent to this (D2s

, D2g

, D3e

) deformation event.

After this period of low differential stress, only localised deformation occurred, suggesting a

heterogeneous stress field. Similarities in microstructures of quartz veins folded in D3s

/D3g

and

deformed in D4e

shearzones suggest that they were deformed under similar conditions. The weakly

developed lattice preferred orientation and incomplete recrystallisation in most veins deformed

during this stage suggest that a steady state microstructure had not developed. Only one quartz vein

in eclogite deformed in a shear zone (D4e2

) shows irregular serrated grain boundaries of quartz and

a strong lattice preferred orientation, suggesting development of a new steady state microstructure

during this deformation. The 10 µm recrystallised grain size indicates a differential stress of ca.

125 MPa (Twiss, 1977) during deformation of this vein. In combination with the “best choice 2”

flow law of Paterson & Luan (1990), this suggests, for the assumed geological strain rates of 10-14-

10-16 s-1, temperatures between 325 and 375 °C (Fig. 26). The localised more intense deformation

(D4e2

), however, could indicate that the deformation was strongly localised (e.g., Küster & Stöckhert,

1999) and the rock deformed with a faster strain rate. This would require higher temperatures

55

during deformation. There is no independent evidence for the temperature during this deformation

stage.

The later deformation stages in the metasedimentary rocks and greenschists (D4s-g

and D5s-g

)

could not be correlated with deformed veins or petrologic information and inferences about PT-

conditions during these deformations are not possible.

6.4 Synthesis: A two stage exhumation for the UHPM rocks of Lago diCignana

A combination of the PT-path with published geochronological data allows an approximate

reconstruction of the PTt-evolution (Fig. 27). An Sm-Nd garnet age of 40.6 ± 2.6 (2 σ) Ma is given

by Amato et al. (1999) for the eclogitic rocks of Lago di Cignana. The closure temperature of the

Sm-Nd system in garnet is ca. 600 °C (Hodges, 1991) and the age of 41 Ma can be considered to

date the UHPM. A similar age, 44.1 ± 0.7 (95 % confidence interval) Ma was obtained with SHRIMP,

U-Pb dating of zircons (closure temperature > 700 °C, Hodges, 1991) in the eclogites (Rubatto et

al., 1998). The later greenschist facies overprint was dated between 40 and 45 Ma with Rb-Sr in

Figure 26

Flow law „best choice 2“ of Paterson & Luan (1990) for dislocation creep in synthetically prepared wetquartzite for geological relevant strain rates of 10-14 and 10-16 s-1. Also depicted are differential stress estimatesfor quartz veins deformed during D

2s and D

4e, as determined with the Twiss (1977) quartz recrystallised

grainsize paleopiezometer. This suggests temperatures between 375 and 450 °C during D2s

and of ca. 330 °Cduring D

4e.

56

newly grown phengites and with U-Pb in titanite by Barnicoat et al. (1995). The fission track ages

in the units above and below the Zermatt Saas eclogites indicate cooling to below 300 - 250 °C

(Tagami & Dumitru, 1996; Wagner et al.,1997) at ca. 33 Ma and cooling to below ca. 125 °C

(Hodges, 1991) at ca. 12 Ma (Hurford et al., 1991).

The earliest exhumation from 2.6 to ca. 0.8 GPa occurred in at maximum 4 m.y. and the minimal

time for this exhumation can be < 1 m.y., because the ages for UHPM and greenschistfacies

Figure 27

Above: Cooling curve calculated for rocks of the Zermatt Saas-Fee zone, calculated with the published agesof Amato et al., (1999), Rubatto et al., (1998), Barnicoat et al., (1995) and Hurford et al., (1991), withclosure temperatures of Hodges (1991).

Below: Decompression curve for the rocks of Lago di Cignana calculated by combining the cooling curve ofthe Zermatt Saas-Fee zone and the PT-path of the rocks fom Lago di Cignana.

57

metamorphism are identical within the limits of error. This results in a minimum average

decompression rate of 450 MPa/m.y. (ca. 15 mm/year for a mean rock density of 3 gr/cm3) and a

maximum average decompression rate of > 1800 MPa/m.y. (> 54 mm/year). The second part of the

exhumation path requires decompression from 0.8 to 0.3 GPa in, at maximum 11 and, at minumum

7 m.y. and results in a minimum average decompression rate of 45 MPa/m.y. (1.3 mm/year) and a

maximum average decompression rate of 70 MPa/m.y. (2.1 mm/year) (Fig. 27).

The large change in decompression rate at pressures around 0.8 GPa, that coincides with a

reorientation of the stress field, indicates a change in the exhumation mechanism at a depth of ca.

25 km for the UHPM rocks of Lago di Cignana. The first exhumation mechanism brings the rocks

very fast (> 8 mm/year) from depths of ca. 90 km to depths of ca. 25 km and with a small decrease

in temperature and low differential stresses. The transition to a different exhumation mechanism

occurs at depths of around 25 km. At this depth, stages with high pore fluid pressures and low

differential stresses alternated with stages with low pore fluid pressures and differential stresses of

up to 40 MPa. The second exhumation mechanism brings the rocks slower (ca. 1-2 mm/year) from

depths of ca. 25 km to depths of ca. 10 km. During this part of the exhumation path the stress field

was very heterogeneous and periods with relatively high (40 to 125 MPa) differential stresses and

low pore fluid pressures alternated with stages with almost lithostatic pore fluid pressure and low

differential stress, as indicated by several generations of late albite veins. For the last part of the

exhumation path, from depths of ca. 10 km to surface conditions, this study provides no constraints.

58

7 Discussion and Exhumation concepts

In this chapter concepts for the exhumation of HPM rocks to normal crustal levels will be intro-

duced and compared to the constraints obtained for the first part of the exhumation path. On this

basis, a tentative scenario for the the two stage exhumation from 90 to ca. 10 km depth of the

UHPM rocks of Lago di Cignana will be proposed.

7.1 Exhumation theories

Before introducing exhumation concepts, some terms must be defined, because exhumation and

uplift are often used in a confusing way in the geological literature (e.g., Behrmann & Ratschbacher,

1989). In this study, exhumation means the vertical movement of rocks with respect to the Earth’s

surface, whereas uplift is vertical movement of rocks or surface with respect to the Geoid (England

& Molnar, 1990). In principle, there are three possible ways to bring rocks closer to the surface:

1. removal of the overburden by erosion,

2. removal of the overburden by extensional tectonic processes,

3. transport of the rocks to the surface in a flowing matrix.

These three exhumation principles are used in all exhumation concepts for HPM rocks and will

be discussed, where relevant, with concepts proposed for the Western Alps as illustration.

7.1.1 Exhumation through erosion

Erosion is an important exhumation process. It is, however, difficult to quantify the effect of

erosion on exhumation. Recent erosion rates are locally upto 13 mm/year, but over a larger area

maximum rates are usually not above 2 mm/year (Allen, 1997). Erosion rates are controlled by

surface elevation and by climate (rainfall) (England & Molnar, 1990; Koons, 1990). The last factor

is often ignored, but may influence erosion rates by one order of magnitude. Surface elevation is

dependent on surface uplift and a high erosion rate can only be maintained, when erosion rate is

approximately balanced by the rate of surface uplift. Therefore, postulation of exhumation through

erosion should always be accompanied by a hypothesis that explains the continuous surface uplift.

Older literature about exhumation in the Western Alps (e.g., Dal Piaz et al., 1971; Hsü, 1991;

Gillet et al., 1985; 1986), usually combines erosion with thrusting, to provide the continuous surface

uplift. These concepts rely heavily on a ca. 100 Ma old ultra high pressure metamorphism at depths

of 80 km or more and a return to midcrustal levels of these HPM rocks at ca. 40 Ma, to be able to

exhume these rocks with reasonable erosion rates. The 41 Ma age for UHPM at Lago di Cignana

(e.g., Amato et al., 1999) requires for the first part of the exhumation path a minimum decompression

rate of 15 mm/year. Therefore, exhumation through erosion is not feasible for the first part of the

exhumation path. It might, however, be important for the second part of the exhumation path with

decompression rates between 1 and 2.1 mm/year.

The concept of Chemenda et al. (1995) differs from the standard concepts, in that it combines

normal faulting with localised erosion and thrusting and only requires locally high erosion rates,

59

Figure 28

Schematic sketches illustrating the exhumation concept of Chemenda et al. (1995). See text for discussion.

but has not yet been applied to the Alps. Chemenda et al. (1995) assume subduction of the continental

crust. When the crust is subducted to depths of approx. 250 km, the buoyant upper crust ”delaminates”

from the weak lower crust and is thrusted on the foreland (Fig. 28A). Ongoing subduction will

further underthrust the continental crust and result in isostatic uplift of this thrust stack and

concomitant erosion. The delaminated upper crust is bounded by two relatively weak zones; the

upper weak zone is the former subduction channel and the lower weak zone is the weak lower crust

or the new subduction channel. The erosional unloading causes this buoyant segment of subducted

upper crust to move upward along the weak lower crust (Fig. 28B). This movement results in faster

movement along the lower thrust and produces normal movement and exhumation along the upper

surface of the slice. However, the low strength of the continental material at UHPM conditions

(Stöckhert & Renner, 1998) precludes the exhumation of large coherent slices of UHPM material

as suggested by Chemenda et al. (1995). Hence, this concept appears unrealistic.

7.1.2 Exhumation by extension tectonics

Exhumation by extension tectonics brings rocks with different metamorphic grade in contact or

will result in large changes of pressure and temperature over a small area. This situation is often

observed in orogens like the Alps (e.g., Selverstone, 1985; Ratschbacher et al, 1989; Blake &

Jayko, 1990), the Franciscan, (Harms et al., 1992), Betics, (Platt & Behrmann, 1986), the Aegean

(e.g., Jolivet et al., 1996; Thomson et al., 1998). This observation alone is not necessarily an indication

for extensional tectonics, because a similar configuration can be obtained by reimbrication of a

nappe pile, or by juxtaposition of rocks that experienced metamorphism at different times (e.g.,

Wheeler & Butler, 1994).

60

Figure 29

The plastic or Coulomb wedge in the concept of Platt(1986, 1987), with terms that describe the geometryof a steady state wedge (modified after Platt, 1993).

For extensional tectonics to take place one has to postulate a period of plate divergence or a

concept to explain extension in a convergent plate tectonic setting. Three concepts exist at present

to explain extension in a convergent plate tectonic setting:

1. the critical wedge (Platt, 1986; 1987).

2. lithospheric extension through gravitational collapse (e.g., Dewey, 1988; England & Houseman,

1989; Lister & Davis, 1989).

3. subduction roll back (e.g., Royden, 1993; Thomson et al., 1998).

These three concepts will be introduced first and concepts that postulate a period of divergence

will be discussed at the end of this section.

7.1.2.1 The critical wedge concept

This concept of Platt (1986; 1987) is based on the work of Chapple (1978), Davis et al. (1983),

and Dahlen et al. (1984) on thrust belts. Platt (1987; 1986) gives a general analysis of an orogenic

wedge with only one rheological assumption, viz. that in a orogenic wedge temperatures and fluid

content will be high enough for ductile flow to occur and to prevent build up of a high stress (e.g.,

Rutter, 1976; 1983; Etheridge, 1983; Atkinson, 1980). Assuming a wedge that has achieved a dynamic

equilibrium, the stable form of the wedge is described by:

τb = ρ g h α

with τb shear stress along the basal decollement, ρ density, g gravity, h thickness of the wedge and

α surface slope (Fig. 29). The significance of this formula is, that it allows to predict the reaction of

the wedge to external modification of its geometry.

If the values of α and/or h are decreased the basal traction exerted by τb (unchanged) is no longer

compensated by the gravity sliding (ρ g h α) and the wedge will shorten. If the wedge shortens αand h become larger and a stable configuration is restored. The values of α and h can be decreased

by erosion at the rear of the wedge or by frontal accretion.

If the values of α and/or h are increased the gravity sliding force (ρ g h α) becomes larger than

the drag force exerted by τb and the wedge will extend. Extension occurs by brittle normal faulting

close to the surface and by horizontal ductile extension at depth. This extension decreases the

values of α and/or h and a stable wedge configuration is restored. The values of α and h can be

increased by underplating at the rear of the wedge or by sedimentation on the wedge.

The combination of underplating below the wedge, with extension in the upper part of the wedge,

elegantly explains formation, preservation and exhumation of HPM rocks. Scenarios for the exhum-

61

Figure 30

Tectonic evolution of the Western Alps after Platt (1987). In the late Cretaceous (70 Ma) upper Penninic andSesia zone rocks have been subducted and experienced HP metamorphism, ongoing subduction of oceaniccrust keeps temperature in these rocks low. Continued underplating till early Oligocene (35 Ma) of lowerPenninic rocks resulted in oversteepening of the wedge and in extension in the overlying Austro-Alpine andupper Penninic rocks, allowing the HPM rocks to rise towards the surface.

ation of the HPM rocks of the Western Alps using this concept are given by Platt (1986) (Fig. 30)

and Polino et al. (1990).

7.1.2.2 The lithospheric extension concept

This is derived from the metamorphic core complex concept (e.g., Lister & Davis, 1989). It

suggests that metamorphic rocks are exhumed through lithospheric extension, involving low-angle

(listric) normal faults (e.g., Lister & Davis, 1989). The concept requires thickening of the continental

lithosphere and isostatic uplift of the surface. The vertical stress generated through this topographic

elevation is balanced by a horizontal stress through continuing convergence. Upsetting of this force

balance in favour of the vertical stress will result in horizontal extension with the development of

low-angle normal faults (e.g., England & Houseman, 1986). The force balance can be disturbed

through removal of a gravitational unstable high density lithospheric root (e.g., England & Houseman,

1989; Dewey, 1988). A variant of this concept is the slab breakoff concept of Davies & von

Blanckenburg (1995), that results in a localised disturbance of the force balance.

62

Figure 31

Schematic diagramm after Royden (1993) showing the response of the upper plate to different relativevelocity configurations of the subducting and overriding plate.

These concepts, however, cannot be used for the exhumation of the HPM rocks of the Western

Alps, because replacement of the relatively cold material at the base of the crust by relatively hot

asthenosphere results in a temperature increase at the base of the crust (e.g., Sonder et al., 1987;

Davies & von Blanckenburg, 1995). The HPM rocks in the Western Alps do, however, not reflect a

significant temperature increase prior or during exhumation (e.g., Schertl et al., 1991, this study).

7.1.2.3 The subduction zone roll back concept

This concept suggests that extension in the upper plate occurs when the subduction rate exceeds

the convergence rate of the plates (Fig. 31). The high subduction rate is thought to be caused by the

slab pull exerted by the sinking of heavy oceanic lithosphere in the mantle (Royden, 1993). Typical

features expected in this situation are, regional extension in the overriding plate, topographical low

mountains and a low erosion rate, low grade to no metamorphism, almost no involvement of

crystalline basement in thrusting and continuous flysch sedimentation (Royden, 1993; Thomson et

al., 1998). The Western Alps clearly do not display these features and therefore, this concept cannot

be used to explain the exhumation of HPM rocks in the Western Alps.

7.1.2.4 Concepts that require a period of divergence

Several authors have attributed exhumation of HPM rocks in the Western Alps through extension,

to a period of divergence between the European and African plates (e.g., Butler, 1986; Ballevre &

Merle, 1993). These scenarios require a middle to late Cretaceous (100- 80 Ma) HP metamorphism

and a period of extension sometime between 80 and 60 Ma (e.g., Butler, 1986; Ballevre & Merle,

63

Figure 32

Simplified cross section illustrating successivepositions and trajectories of identifiable points inthe dynamic scaled wedge model of Cowan &Silling (1978).

1993) to partly exhume these HPM rocks. The newer radiometric ages between 70 and 35 Ma (e.g.,

Inger et al., 1996; Gebauer et al., 1997) for the UHP metamorphism leave, however, not enough

time for a period of plate divergence to exhume HPM rocks.

7.1.3 Upflow concepts

Exhumation by upflow requires the high pressure metamorphic rocks to be embedded in a low

viscosity matrix (Cloos, 1982; Emerman & Turcotte, 1983; Platt, 1993). The HPM rocks themselves

cannot have a low viscosity, because the intense deformation that low viscous rock would experience

during exhumation, would probably result in complete reequilibration of the mineral paragenesis

(e.g., Rutter & Brodie, 1985). Two endmember flow processes can be postulated:

· Buoyant upflow of material driven by density contrasts.

· Upflow of material driven by forced flow.

The first process requires that the high pressure rocks and their matrix have a relatively low bulk

density compared to the surrounding rocks. It was proposed by England & Holland (1979) to exhume

eclogitic blocks in a carbonate rich matrix and by Takasu (1989) to exhume blocks of HPM rocks in

a serpentinite matrix. This mechanism cannot be used to exhume continuous large sections of HPM

rocks.

The second process is based on the corner flow concept of Cowan & Silling (1978), who used a

dynamic scaled model to study the development of an accretionary prism. They found the expected

underthrusting at the toe of the prism (e.g., Karig, 1974), but also that appreciable amounts of

sediments were carried below the wedge and were accreted there, and that material began to flow

upward from the deepest part of the accretionary prism (Fig. 32). If the rocks in an accretionary

prism behave as a viscous fluid, this forced flow could bring material from the deepest part of the

accretionary prism to shallower levels in the wedge. This can be considered as an initial stage in the

development of an accretionary wedge that, with ongoing subduction and accretion, will develop in

a critical tapered wedge (e.g., Platt, 1986; 1987).

The subduction channel concept is a modification of the corner flow model for a narrowing

channel and was proposed by Cloos (1982) to explain observations in the Franciscan subduction

complex. It was further developed (Shreve & Cloos, 1986; Cloos & Shreve, 1988 a; 1988b) to

describe the processes of prism accretion, sediment subduction and melange formation.

The concept assumes that subducting sediments deform approximately as a viscous fluid, when

they are dragged by the descending plate beneath the overriding plate and the accretionary prism.

This layer of deforming sediments forms a shear zone, called the subduction channel. The subduction

64

channel has a certain width, that depends on the velocity and angle of subduction, as well as on

surface slope and material in the hanging wall. The width of the subduction channel determines its

capacity, the amount of sediment that can be transported downwards along the subduction channel.

If enough sediment is available at the inlet of the subduction channel, it will be filled to capacity.

Where the dip of the descending plate changes or where the rear of an accretionary wedge abuts

basement rock the subduction channel changes its width (control point). At the control point the

capacity of the subduction channel decreases. If the subduction channel was filled to capacity, not

all incoming material can pass the control point. Material will accumulate at the control point and

the channel thickens. When this happens, the upward directed force due the adverse pressure gradient

and the buoyancy of the sediment, becomes larger as the downward directed force due to shearing

and a zone of reverse flow or upflow will develop. The material that flows up consists of low

viscous metasedimentary rocks that are intensely deformed. In this low viscous matrix, small blocks

of high viscous material that have retained their HPM imprint, that is almost completely wiped out

in the low viscous material, can be included and brought to shallow crustal levels (concept of

Cloos, 1982). The flowing material exerts a viscous drag (shear stress) on the walls of the channel

(Shreve & Cloos, 1986). Without reverse flow this viscous drag is downward directed for the hanging

wall and can result in incorporation of hanging wall material in the subduction channel (subduction

erosion). In a zone of reverse flow the viscous drag on the hanging wall is upward directed and

could move larger sheets of previously accreted (HPM) rocks to the surface (Cloos & Shreve,

1988a).

The weak point of the subduction channel concept is the nature and the deformation mechanism

of the low viscous material in the channel. In the quantitative subduction channel models of Shreve

& Cloos (1986), water saturated sediment is taken as the low viscosity material. This may be valid

for the upper few kilometres of the subduction channel, but at depths of 90 km or more, necessary

to exhume UHPM rocks with this concept, a different yet unspecified material and deformation

mechanism operating in this material are required.

Forced flow concepts were proposed to explain the exhumation of (U)HPM rocks in the Western

Alps by Fry & Barnicoat (1987) for the Zermatt Saas zone and by Michard et al. (1993) for the Dora

Maira Massif. The interpretation of Michard et al. (1993) postulates, the oldest HP metamorphism

for ca. 100 Ma old and a period of ca. 60 m.y. of subduction, but can be readily adapted to younger

HP metamorphism and a shorter subduction time span.

These concepts (Fig. 33) assume onset of subduction of oceanic crust (rocks of the Zermatt Saas

zone) with offscraping of parts of the southern continent (Sesia zone). To accrete parts of the sub-

ducting oceanic crust to the overlying plate, Fry & Barnicoat (1987) suggest geometric irregularities

along the subducting slab or rheological irregularities in the slab, to cause detachment from the

subducting slab. With the onset of continental collision, fragments of the thinned continental margin

(Monte Rosa, Dora Maira) are also subducted. The density contrast between the deeply subducted

continental rocks (3.09 gr/cm3) and the surrounding mantle rocks (3.3 gr/cm3) adds buoyant uprise

to the forces that can cause detachment from the subducting slab and accretion to the overlying

65

plate (Michard et al., 1993). Exhumation occurs by forced return flow in a narrowing subduction

channel driven by continuing continental collision. During exhumation UHPM rocks become mixed

with rocks that experienced HP metamorphism at lower pressures (Michard et al., 1993). After

forced flow exhumation to mid crustal levels, further exhumation was achieved by other mechanisms.

7.2 Evaluation of published exhumation scenarios for exhumation fromdepths of approx. 90 km to 30 km

Only the upflow (e.g., Fry & Barnicoat, 1987; Michard et al., 1993) and the critical wedge (Platt,

1986; 1987) concepts, stay within the limits posed by the PTD-path of this study and geochronological

data (e.g., Amato et al., 1999; Barnicoat et al., 1995). Essential for a scenario that uses extensional

tectonics to explain the exhumation of HPM rocks, is the identification of extensional structures

that were active during the exhumation of the HPM rocks. In the area around Valtournanche the

only described extensional structure is the ”Combin fault”, that is considered part of the Mischabel

backfold/backthrust system (e.g., Wheeler & Butler, 1993; Barnicoat et al., 1995). On this fault

system extensional activity under lower greenschist facies PT-conditions took place at ca. 40 Ma

(Barnicoat et al., 1995), post-dating the greenschist facies overprint of the HPM rocks in the Zermatt

area (Barnicoat et al., 1995). Therefore, this structure was active as the HPM rocks of the Zermatt

Saas zone were already at a midcrustal level. In its present configuration this fault cannot be

responsible for the exhumation of the HPM rocks. As long as from the Northern part of the Western

Alps no extensional structures are described, that predate the greenschist facies overprint of the

HPM rocks, the critical wedge model of Platt (1986; 1987) is not applicable to the exhumation of

the UHPM rocks of Lago di Cignana.

The forced flow concept requires that during exhumation, the UHPM rocks are embedded in a

matrix of low viscous material that precludes the buildup of higher differential stresses at depth in

the subduction channel (Shreve & Cloos, 1986). Low differential stresses at depth in subduction

zones are inferred from geological evidence (e.g., Stöckhert et al., 1997; 1999) and from geophysical

reasoning (e.g., Pacheco et al., 1993; Wang et al., 1995). The nature of the material in the subduction

channel and the deformation processes operating in this material are unknown (e.g., Platt, 1993). At

Lago di Cignana the serpentinites, that occur in large volumes in the Zermatt Saas zone and the

locally preserved HP metasedimentary rocks of the Zermatt Saas zone, could have been these low

viscosity rocks. The metasedimentary rocks of the Zermatt Saas zone consist mainly of quartz-

phengite-garnet schists, that locally have preserved their HPM imprint as inclusions in rigid minerals

(e.g., Reinecke, 1995). During the later exhumation, however, microstructures in the rock were

completely modified and inferences about deformation processes during UHPM conditions can no

longer be made. The same holds for the serpentinites that have preserved deformation structures

(e.g., Vogler, 1987), but because of the PT insensitive mineral paragenesis, these cannot be unequivo-

cally attributed to specific segments of the PT-path.

A subduction channel is characterised by high strain rates at relatively low temperatures and the

deformation process operating should preclude high differential stresses. Most geologic materials

66

require for deformation by dislocation creep at these conditions (e.g., Carter & Tsenn, 1986),

differential stresses that are much too high for the postulated viscosities (10-17-10-18 Pa s, Shreve &

Cloos, 1986). Altough most minerals in crustal rocks deforming by dislocation creep are weaker

then expected (Stöckhert & Renner, 1998), they are still not weak enough. Diffusional flow

deformation mechanisms can achieve deformation at low differential stress, but at the relatively

low temperature conditions only diffusion precipitation creep in the presence of a fluid phase is a

feasible mechanism. Stöckhert et al. (1999) estimated for the HPM phyllite quarzite unit of Crete,

which deformed mainly by dissolution precipitation creep (Schwarz & Stöckhert, 1996), a bulk vis-

cosity of ca. 10–19 Pa s, still a factor 10 higher as the viscosity in normal subduction channel models

(e.g., Shreve & Cloos, 1986), although Mancktelow (1995) used viscosities between 10-17-10-19 Pa

s to model tectonic overpressures in a subduction channel setting. A deformation process, similar to

liquid phase sintering is considered feasible to explain the inferred low strenghth of UHPM rocks

by Stöckhert & Renner (1998), but microstructural evidence in geologic materials for this process

has not yet been presented.

Although the nature of the material and the deformation mechanism operating in this material in

the subduction channel are not unequivocally identified, a forced flow subduction channel concept

can be applied to explain the exhumation from 90 km to 25 km depth of the UHPM rocks of Lago

di Cignana. A forced flow subduction channel scenario for the UHPM rocks of Lago di Cignana

will be presented and discussed in the next section.

7.3 Scenario for exhumation from ca. 90 km to ca. 25 km depth

In a forced flow subduction channel scenario for the UHPM rocks of Lago di Cignana, several

points must be discussed. A short description of the scenario is given and the numbered points will

be discussed.

The oceanic crust at Lago di Cignana was subducted down to depths of ca. 90 km. Deformation

during subduction was concentrated in the weak subduction channel above the oceanic crust (Fig. 33).

At this depth, a part of the oceanic crust was detached from the downgoing slab (1) and incorporated

in the subduction channel. Assumming a control point in ca. 90 km depth (2) and a subduction

channel filled over the capacity of the control point (3), the oceanic slab was transported upward

along the subduction channel (4) through a forced return flow in a low viscous material. Where the

drag force of the hanging wall became larger than the driving force of the return flow, the material

was either accreted to the hanging wall (5) or the material flowed down again.

Point (1), detachment of the downgoing plate, requires localised deformation of the downgoing

slab at or close to maximum PT-conditions. At first, this seems to contradict the subduction channel

model, because deformation is assummed to be concentrated in the weak material of the subduction

channel. The record of the eclogites at Lago di Cignana, however, shows at maximum PT-conditions

deformation of the rock by dislocation creep of omphacite. At these conditions jadeite may flow at

differential stresses of a few MPa (Stöckhert & Renner, 1998) and omphacite probably flows at

somewhat higher stresses. This is a similar magnitude as the differential stress that in subduction

67

Figure 33

A tentative schematic sketch illustrating some important points of the proposed exhumation scenario for theUHPM rocks of Lago di Cignana.

The upper sketches show the configuration at UHPM conditions before exhumation. In the right sketch thesituation in the subduction channel is shown. The velocity distribution in the subduction channel is qualitativelyonly and adapted from England & Holland (1979). ∆-velocity is the difference between the velocity of thedowngoing plate and the material in the subduction channel close to the plate-channel interface and a measurefor the magnitude of the viscous drag, that is assummed to have caused deformation by dislocation creep inomphacite. Localisation of deformation results in the development of a shearzone in the downgoing plateand in detachment of UHP metamorphic rocks from this plate.

The lower sketches show the configuration at the onset of exhumation. The right sketch shows the situationin the subduction channel at the control point. The width of the subduction channel at the control point,determines the amount of material that can pass. In the sketch, all material below the dashed line can passthe control point and is subducted. Material between the dashed and dotted lines is downflowing material inthe subduction channel, that cannot pass the control point and will follow a path given by the arrow. Betweendotted line and the mantle wedge of the overlying plate a zone of reverse flow occurs, that allows forexhumation of material.

channel models (e.g., Shreve & Cloos, 1986) is produced by viscous drag of the flowing material

on the walls of the channel. The magnitude of the viscous drag in these models depends on the

vicosity of the material in the subduction channel, the channel width, the velocity of the downgoing

plate, and on the change in hydraulic potential and channel width in direction of subduction (Shreve

& Cloos, 1986). Most of these parameters are only approximately known, but varying the parameters

within reasonable limits (factor 10 higher or lower viscosities, plate velocities between 1 and

10 cm/year, subduction channel thickness between 300-5000 m) gives similar magnitudes for the

differential stress (e.g., Shreve & Cloos, 1986; Mancktelow, 1995). This suggests that at maximum

PT-conditions the eclogites at Lago di Cignana were deformed, because of the viscous drag of the

68

material flowing in the subduction channel on the downgoing plate. Detachment of the rocks from

the downgoing plate requires localisation of the deformation in a shear zone below these rocks. The

heterogeneous deformation at UHPM conditions at Lago di Cignana (this study) is also observed at

other UHPM localities (e.g., Michard et al., 1993; 1995), therefore, localisation of deformation has

to be expected. Because the shear zone rocks could not be identified, nothing can be said about

deformation mechanisms in the shear zone. Possible mechanisms are dissolution precipitation creep

as inferred from microstructures by Stöckhert et al., (1997) for rocks from the Tauern Window

deformed under HPM conditions or grain size sensitive flow that, however, would require an extreme

grainsize reduction in the shear zone (e.g., Walker et al., 1990).

Point (2) concerns the control point in ca. 90 km depth. At the control point, the width of the

subduction channel changes. Cloos & Shreve (1988a; 1988b) propose a change of material in the

overlying plate (e.g. accretionary wedge to crystalline basement) or a change of dip in the downgoing

plate as possible causes for the development of a control point. The only possible material change

in the overlying plate in this depth range is the crust mantle transition. Present day crustal thickness

in mountain belts, however, rarely exceeds 70 km (e.g., Tanimoto, 1995) and a crustal thickness of

90 km implies extreme thickening of the overlying plate and this seems improbable, because large

scale continental collision is considered to occur later (e.g., Steck & Hunziker, 1994). The alternative

is, that the downgoing plate changes its dip at ca. 90 km depth. According to Jarrard (1986), the

greatest change in dip in the downgoing plates in present day subduction zones occurs between

depths of 60 and 100 km. From his data, it is not clear which parameter influence the depth of the

dip change, therefore, it cannot be ascertained whether or not the plate tectonic configuration of the

Western Alps at ca. 44 Ma could produce a change of dip in the downgoing plate at approx. 90 km

depth. It is, however, the most probable explanation for the existence of a control point at approx.

90 km depth.

Point (3) is concerned with the amount of material in the subduction channel above the control

point. If this amount is smaller than the capacity at the control point, return flow and exhumation

cannot occurr. The amount of material in the subduction channel cannot be estimated. The schistes

lustres or Bundnerschiefer (calcschists and greenschists of the Combin zone), however, are interpreted

to have formed in an accretionary wedge (e.g., Deville et al., 1992). The formation of an accretionary

wedge requires a certain amount of sediment on the downgoing plate (e.g., Pavlis & Bruhn, 1983).

This does not prove that parts of this sediments were subducted to great depths, but it shows at least

that at shallower depths enough material was available to fill the subduction channel to capacity

(e.g., Cloos & Shreve, 1988b).

Point (4), the upward transport along the subduction channel in a matrix of low viscous rocks,

explains the almost isothermal decompression with slight cooling and no notable deformation, as

recorded in the UHPM rocks of Lago di Cignana, because thermal models for subduction zones

(e.g., Peacock, 1987; 1996), show that isotherms are subparallel to the subduction channel. These

models, however, cannot be quantitatively applied, because they do not account for the return flow

of material. Qualitatively the return flow of hotter material from below, will result in higher

69

temperatures at given depth as expected from thermal modelling without return flow. The magnitude

of this temperature rise will depend on the velocity and the amount of material flowing back. The

presence of cold material below the zone of return flow, will qualitatively result in cooling of this

material during exhumation, as for example recorded by the rocks of Lago di Cignana.

Point (5) is the accretion of the upward transported slice of UHPM material to the hanging wall.

The material in the hanging wall has a non-negligible strength and can transmit higher stresses.

This results in deformation of the accreted rock during further exhumation as described for example

by Stöckhert et al. (1997) for HPM rocks of the Tauern window. The change in decompression rate

in the UHPM rocks of Lago di Cignana that coincides with a change in orientation of the stress field

and an increase in maximum differential stress, suggests that the rocks became accreted to the

overlying plate at temperatures of ca. 500 °C and a depth of ca. 25 km.

7.4 The scenario for the later exhumation from depths of ca. 25 km to thesurface

This part of the exhumation path is also divided in two parts, exhumation from depths of ca.

25 km to depths of ca. 10 km and from there towards the surface. For this last part, this study offers

no constraints and it will not be discussed.

A comparison with published data for the Northwestern Alps (e.g., Mazurek, 1986; Ellis et al.,

1989; Wust & Silverberg, 1989; Sartori, 1990; Wheeler & Butler, 1993; Barnicoat et al., 1995)

allows the integration of the data of Lago di Cignana in the regional framework and the development

of an exhumation scenario for this part of the exhumation path. Formation of the greenschists (D3e

)

in the metabasic and D2s

in the metasedimentary rocks are tentatively correlated with top to the NW

movement of several regional faults under greenschist facies conditions (e.g., Ellis et al., 1989;

Barnicoat et al., 1995). This deformation is related to the onset of nappe stacking due to SE directed

underthrusting of the European continental crust below the Adriatic or Apulian continental crust

(e.g., Butler, 1986; Steck & Hunziker, 1994). In this thrusting event that occurred between 43 Ma

(age of static greenschist facies overprint, Barnicoat et al., 1995) and 40 Ma (age of SE directed

fault zone, Barnicoat et al., 1995), the rocks of the Zermatt Saas zone were juxtaposed between the

rocks of the Monte Rosa unit and the rocks of the Combin zone (Fig. 34A). The thrusts bounding

the Zermatt Saas zone then became inactive and new thrusts developed further north.

The localised D3s

and D4e

deformation at Lago di Cignana is tentatively correlated with top to the

SE movement. This late top to the SE movement is traditionally interpreted as backthrusting or

backfolding (e.g., Steck, 1990; Sartori, 1987), because it often stacks external units on top of internal

units. Recently, some late structures with top to the SE and E displacement have been interpreted as

hinterland dipping extensional shearzones (e.g., Phillipot, 1990; Wheeler & Butler, 1993). The

contradictionary interpretations for these shearzones, result from possible reorientation of these

structures through later deformation (Wheeler & Butler, 1993). If these shears are interpreted as

backthrusts (e.g., Steck, 1994), the main exhumation mechanism must have been erosion, which

would require relative high erosion rates (Allen, 1997) of between 2 and 3 mm/year. Therefore, I

70

Figure 34

A tentative schematic sketch illustrating the proposed exhumation scenario for the UHPM rocks of Lago diCignana from depths of 25 km to ca. 10 km.

The upper sketches show the configuration just after breakoff of the oceanic crustal slab (see text fordiscussion). The crust at the former subduction zone was already thickened by thrusting and is furtherthickened by buoyant uprise of deeply subducted slabs of continental material along former thrusts. Theright sketch shows, that at this stage the already exhumed UHPM rocks in the subduction channel material,become juxtaposed between underthrusted continental crust (Monte Rosa unit) and serpentinites and materialfrom the accretionary wedge (Combin zone).

The lower sketches shows the proposed exhumation scenario. See text for discussion. During extensionalshearing, favourably orientated thrust were reactivated as low angle normal faults. Where thrusts were notfavourably orientated they were cut off by low angle normal faults.

prefer to interpret most of theses shears as extensional shears. A tentative interpretation of these top

to the SE shears as extensional shearzones in combination with top to the NW thrusting after the

interpretation of Wheeler & Butler (1993) is shown in figure 34B.

The described features can be explained in a scenario that combines features from the critical

wedge concept of Platt (1986; 1987) and the slab breakoff concept of von Blankenburg & Davies

(1995). Prior to subduction of buoyant continental crust, slab pull of the downgoing slab is the

force, that mainly determines the configuration of a subduction zone (e.g., Royden, 1993). With the

onset of subduction of continental crust, buoyancy disturbs the force balance and will lead to a

changed stress situation in the downgoing slab. Ultimately, the heavy oceanic slab will break off

(Davies & von Blanckenburg, 1995). Because further subduction of buoyant continental crust is not

possible, the ongoing convergence between the plates must be accommodated otherwise. The inter-

face between continental crust (quartzo-feldspatic rocks) and mantle (olivine rocks) is, due to the

compositional change, also a rheologic interface between relatively weak crustal rocks and strong

71

mantle rocks (e.g., Kusznir & Park, 1986). Therefore, crust and mantle can decouple along this

interface (e.g., van den Beukel, 1992). With ongoing convergence the mantle part of the lithosphere

will be subducted and convergence in the crust is taken up by thrusting (e.g., Laubscher, 1990). At

the same time, however, already subducted continental crust, rises along the subduction zone, and

this results in extreme thickening of the crust and in reorientation of the older thrust surfaces, which

are no longer favourably orientated for thrusting. Further shortening of the crust is taken up in new

thrust zones that developed further to the North. The thickening of the continental crust results in

isostatic uplift of the surface. The vertical stress generated by this uplift is, however, no longer

balanced by a horizontal stress and the result is horizontal extension with the development of low-

angle normal faults (e.g., von Blanckenburg & Davies, 1994).

For the exhumation from a depth of ca. 10 km as the rocks had a temperature close to 300 °C to

surface conditions, this study offers no constraints. Discontinuous uplift of discrete blocks with

different erosion rates caused by dextral transpression is discussed as possibility in the literature

(e.g., Laubscher, 1990; Hurford et al., 1991; Steck & Hunziker, 1994; Escher et al., 1997; Marchant

& Stampfli, 1997).

72

8 Conclusions

The PTD- path for the exhumation of UHPM rocks of Lago di Cignana can be partly reconstructed

by combining petrological and (micro)structural observations. This PTD-path combined with

published radiometric ages, divides the exhumation history in two parts. The first part of the

exhumation is very fast, almost isothermal decompression from depths of approx. 90 km to depths

of approx. 25 km, with differential stresses too low to drive deformation in the metabasic rocks. At

around 500 °C and 0.8 GPa, the slope of the PT-path as well as the orientation of the stress field

changes. The second part of the exhumation is slower, with pronounced cooling during uplift from

depths of approx. 25 km to depths of approx. 10 km and deformation at higher differential stresses.

The exhumation mechanism for this first part of the exhumation path that obeys most constraints

imposed by the PTDt-path is a modified forced flow/subduction channel model, as proposed by

Shreve & Cloos (1986) and Cloos & Shreve (1988 a; 1988b). For the second part of the exhumation

path a modified slab break off model (e.g., Davies & von Blanckenburg, 1995) is feasible.

For the UHPM rocks of Lago di Cignana following scenario is considered. The oceanic rocks

were subducted to depths of about 90 km and metamorphosed at pressures of 2.6-2.8 GPa and a

temperature of ca. 600 °C. Under these conditions, the eclogites were heterogeneously deformed

with differential stresses, high enough to drive deformation by dislocation creep in omphacite. This

deformation is tentatively attributed to the viscous drag between the material flowing in the subduction

channel and the foot wall. At these conditions the material must have been transferred from the

downgoing plate to the subduction channel, possibly by further localisation of deformation in a

shear zone that is no longer preserved. Subsequently, differential stress was too low to drive further

deformation in the metabasic rocks. Exhumation of the slice of UHP material to depths of approx.

25 km is attributed to a forced return flow in a matrix of weak material. For the forced return flow

to occur a control point at approx. 90 km depth has to be assummed.

Accretion of the slice of UHP material to the hanging wall occured at a depth of approx. 25 km

and a temperature of ca. 500 °C. Accretion was closely followed by wholesale continent-continent

collision. At this stage the subduction channel became inactive and the Zermatt Saas zone probably

became a coherent unit, composed of several subunits that had followed slightly different PT-paths

before (e.g., Ellis et al., 1989; Barnicoat & Fry, 1986; Meyer, 1983; Reinecke, 1991; 1995; this

study). After accretion, higher stresses were possible, resulting in development of the greenschists

in the metabasic rocks and intensive deformation D2s in the metasedimentary rocks. This deformation

is correlated with NW directed overthrusting under greenschistfacies conditions between 43 and

40 Ma (Barnicoat et al., 1995).

Exhumation of the UHPM rocks from Lago di Cignana from depths of ca. 25 km to depths of ca.

10 km between 40 and 33 Ma under lower greenschist facies conditions is attributed to hinterland-

directed shears (e.g., Steck & Hunziker, 1994; Wheeler & Butler, 1993), that are tentatively correlated

with the late localised deformation in the rocks of Lago di Cignana.

73

An important objekt for further study are the deformation mechanisms in the weak material in

the subduction channel. Stöckhert & Renner (1998) propose a mechanism similar to liquid phase

sintering in the presence of a highly saline fluid phase or a melt, as possible deformation mechanism,

but also state that microstructures indicative for this process have not been observed and that

experimental evidence on geologic materials for this mechanism is also not available.

Another subject is the regional study of structures, active under greenschist facies conditions

and with top to the SE movement. These structures are traditionally interpreted as backthrusts (e.g.,

Steck & Hunziker, 1994), but must be reeinterpreted as rotated extensional shear zones (e.g., Wheeler

& Butler, 1993) to validate the postulated model for exhumation from 25 to 10 km depth.

74

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Lebenslauf

Name: Sebastiaan Nicolaas Gerardus Cornelis van der Klauw

Geburtsdatum: 28. September 1966

Geburtsort: Gouda

Staatsangehörigkeit: Niederländisch

Familienstand: Ledig

Akademischer Werdegang

08.78 - 05.84 St. Willibrord Gymnasium in Deurne

05.84 Abitur

09.84 - 11.90 Geologiestudium an der Rijksuniversiteit Utrecht

30.11.90 Examen zum Diplom-Geologen

04.91 - 03.94 Wissenschaftlicher Mitarbeiter am Institut für Geologie der Ruhr-Universität

Bochum (Promotionsstelle)

04.94 - 09.94 Wissenschaftlicher Hilfskraft am Institut für Geologie der Ruhr-Universität

Bochum

04.96 - Wissenschaftlicher Mitarbeiter am Institut für Geowissenschaften des

Friedrich-Schiller-Universität Jena

A-1Appendix A methods

APPENDIX A Methods

A1 Sampling

Mapping in the area around Lago di Cignana (unpublished Diplomkartierung, Habermann, 1992,

Wagner-Zweigel, 1993) showed that the UHPM rocks are extremely well exposed on the southern

shore of the lake. All of the about 120 samples (Table C1) for this study were taken from this well

exposed area (Fig. A1). Due to these good exposures the lower PT-overprint could be correlated

with m- to dm- scale structures in the metabasic rocks and several series of samples were taken to

investigate the relation between structures and lower PT-overprint. Due to the very heterogeneous

bulk rock composition of the metasedimentary rocks, such a correlation was not possible for that

material and sampling was concentrated on small scale folds and veins.

A2 Preparation

From all samples thin sections were made to study with a polarising microscope; usually one

thin section was made approximately parallel to the stretching lineation and normal to the foliation,

and another thin section normal to the stretching lineation and the foliation. In samples with no

apparent stretching lineation a thin section normal to the foliation was cut. From vein samples, thin

sections with both vein and host rock were made.

Figure A1

Distribution of the different lithologies at the southern shore of Lago di Cignana.

Appendix A methodsA-2

A small part of most samples was finely grounded for investigation with X-ray diffractometry to

distinguish between paragonitic and phengitic white mica. From selected samples thin sections

polished on both sides and without cover slip were made for investigation with the electron

microprobe (EMP, Table C3 -C22), Scanning electron microscope (SEM) and cathodoluminesence

microscope (CL). From several vein samples, 200 µm thick sections were made for the investigation

of fluid inclusions by microthermometry. After study of the thin sections a series of seven samples

from fresh (group 1) to completely overprinted (group 4) eclogite was selected for X-ray fluorescence

(XRF) whole rock chemistry (Table C2).

A3 Analytical methods

In order to determine the phases and their compositions in the metabasic and the metasedimentary

rocks as well as to determine the relative volumes and shape preferred orientations of some of these

phases, and for fluid inclusion studies, the following analytical methods were used:

· polarising microscopy

· powder X-ray diffractometry

· electron microprobe analysis

· X-ray fluorescence spectroscopy,

· scanning electron microscopy,

· cathodoluminesence microscopy

· image analysis

· microthermometry

A3.1 Polarising microscopy

A polarising microscope allows determination of phases present in a thin section and also to

establish the spatial relations between these phases. Furthermore, it allows observation of deformation

microstructures for the different phases.

Polarising microscopes of Zeiss, Leitz and Olympus were used in this study. Important

observations were photographed with an Olympus OM 10 camera mounted on an Olympus polarising

microscope. A Leitz microscope with long working distance objectives was used for Universal

stage measurements.

A3.2 powder X- ray diffraction

For powder X-ray diffraction a representative part of the sample is finely grounded (1- 10 µm),

to obtain a large amount of grains of the different minerals, so that it is likely that all grain orientations

for all minerals are present. The powdered specimen is brought into a beam of monochromatic

parallel X-rays and slowly rotated. The incident X-rays will be scattered by the atomic planes in the

specimen. These diffracted X-rays will usually interfere destructively with each other and no signal

will be produced. For specific incedent angles however, the spacing of the atomic planes is such,


that the diffracted X-rays interfere positively with each other and a signal can be recorded. This is

Braggs law, in formula

n λ = 2 d sinθwith λ wavelength of the X-rays, d distance between the atomic planes, θ incident angle of the X-

ray beam and n an integer (usually taken as 1). When the wavelength of the X-rays is known and the

different incident angles at which a signal occurred are recorded, the d values for the unknown

specimen may be calculated. These d-values together with the intensities of the signals are material

specific. By comparing the recorded values with reference values in the A.S.T.M. powder data file,

the unknown material(s) may be identified. More information on X-ray diffraction may be found in

Zussmann (1977) and Putnis (1992).

Philips X-ray diffractometers at the “Institut für Mineralogie” and the “ Institut für Geologie” at the

Ruhr-University Bochum were used in this study. All scans were made with Cu Kα X-rays over a

range of θ angles from 5° to 50° with steps of 0.1° and 2 seconds counting time.

A3.3 Electron microprobe and X-ray fluorescence spectroscopy

Electron microprobe and X-ray fluorescence use the same principles, but different excitating

media to produce X-rays. When an electron with sufficient energy strikes matter, X-rays are produced.

X-rays may also be produced, when these primary X-rays strike matter. These secondary X-rays are

called fluorescence. The X-ray spectrum produced by incedent electrons may be divided in a

continuous spectrum (background) and a characteristic spectrum. Excitation by primary X-rays

differs from excitation by electrons in that no continuous spectrum is formed. The characteristic

spectrum is produced when the incident electrons remove an electron from the inner shells of an

atom. The X-ray photons that are produced when outer electrons fall back have an energy that is

characteristic for a particular element. The energies (or wavelengths) and intensities of the excited

X-rays are measured in a spectrometer. From the measured wavelengths the different elements that

are present in the material can be inferred. By comparing the intensities of the X-rays with intensities

obtained from materials with known composition, the absolute amounts of the different elements

may be obtained. More about these techniques may be found in Zussman (1977), Smith (1976), and

Reed (1996).

A3.3.1 The electron microprobe (EMP)

The EMP uses a beam of electrons to produce characteristic X-rays. This beam is focused using

magnetic lenses, without loss of intensity. Therefore, the electron microprobe can be used to obtain

spot analyses (1 µm diameter) from a material. However due to the superposition of continuous and

characteristic X-ray spectra the accuracy of the EMP is not as high as the accuracy of the XRF. To

prevent the build up of heat and electrical charge on the specimen, samples must be coated with a

conductive thin carbon or gold film. In this study the electron microprobe was used to measure the

composition of minerals in thin section in specific microstructural settings.

A Camebax microprobe in WDS mode at the “Bereich Zentrale Elektronen-Mikrosonde” of the

Ruhr-University Bochum was used. Operating conditions were 15 kV accelerating voltage and a

Appendix A methodsA-4

14 nA beam current for most minerals. For albite and mica the beam was slightly defocused and a

12 nA beam current was used to yield better results for the alkali elements. A 12 nA beam current

was also used for carbonates. Natural and synthetic minerals were used as standards and the PAP

(Pouchou & Pichoir, 1984) correction procedure was used.

A3.3.2 X-ray fluorescence spectroscopy (XRF)

X-ray fluorescence spectroscopy uses X-rays to produce characteristic X-rays. X-rays cannot be

focused without loss of intensity. Therefore, XRF gives information about the composition of a

larger area. To ensure that this area is homogeneous and representative of the sample, part of the

sample is dissolved in lithium borate glass and the glass is analysed or the sample is finely grounded

and a pressed powder tablet is analysed. These analyses give information about the bulk composition

of a sample. A more detailed description of the XRF technique can be found in Zussmann (1977).

A Philips PW 1400 X-ray fluoresence spectrometer at the “Institut für Mineralogie” at the Ruhr

university Bochum was used for XRF-analyses.

A3.4 Scanning electron microscopy (SEM)

When electrons with sufficient energy strike matter, not only X-rays are produced but also other

signals. In the SEM, the signals provided by the backscattered electrons and the secondary electrons

are used. Secondary electrons are the electrons that are removed from the electron shells around an

atom by the incident electrons. Their energy ranges from 0 to about 50 eV, partly depending on the

material. Backscattered electrons are electrons of the incident beam that are rebounded in the

specimen. They have generally higher energies than the secondary electrons, ranging between zero

and the energy of the incident electrons. Their intensity is related to the mean atomic number of the

material under the beam. Both signals can be detected when they leave the surface of the specimen

and give information about the surface topography of the sample and some qualitative information

about the material under the beam. When the sample has a smooth surface the SEM can be used

much the same way as a normal light optical microscope, with the advantages that the range of

possible magnification is larger and that SEM has a better depth of focus. More information about

this technique can be found in Reed (1996).

In this study SEM was used to provide images of the symplectitic intergrowths in the metabasic

rocks. SEM images were made with a Cambridge Stereoscan 250 Mk III at the “Bereich Zentrales

Rasterelektronenmikroskop” of the Ruhr University Bochum. Accelerating voltage for the

electronbeam varied between 15 and 20 kV. SEM images were made with assistance of Dr. Neuser.

A3.5 Cathodoluminescence (CL)

Another signal that may be emitted when a material is struck by electrons is light in the visible

wavelength area. This may be an intrinsic property of the material under the beam, for example in

scheelite or benthonite, but may also be due to the presence of trace impurities in the mineral e.g.,

Mn and REE in calcite or defects in crystal structure e.g., quartz (Marshall, 1988).

In this study CL was used to image the zoning of calcite around dolomite, that could not be seen


in polarisation microscope. A cathodoluminescence microscope HC1-LM at the “Institut für

Geowissenschaften Ruhr Universität Bochum”, developed by Dr. Neuser (Neuser, 1995) was used

in this study. A standard camera mounted on the microscope was used to obtain photographs of the

CL-images. Dr. Neuser and Dipl.-Geol Habermann assisted with the CL investigations.

A3.6 Image analysis

Image analysis was used to obtain qualitative information on shape, area, and shape preferred

orientation of minerals in thin sections or on back scattered electron images. The image is digitised

and a computer program approximates area, perimeter, longest dimension, direction of longest

dimension, and other parameters from this image.

The VIDS IV image analysis system (AI-Tektron) combined with a videocamera (JVC BY-110)

mounted on a Zeiss microscope and a digitising tablet were used in this study.

A3.7 Microthermometry

With the microthermometry it is possible to obtain information about density and composition

of fluid inclusions without destroying the inclusions. A heating-freezing stage installed on a

microscope allows to observe phase transitions in the fluid inclusionsas a function of temperature.

Two heating-freezing stages were used, a Linkam THM 600, described in Sheperd (1981) and

Roedder (1984) and a stage specially for low temperature measurements, constructed by W. Harbott

at the “Institut für Geologie der Ruhr Universität Bochum”. This last stage is described by Harbott

et al. (1990) and Küster (1994).

Both stages were calibrated with natural standards (e.g. Calanda Quartz provided by J. Mullis)

in the low temperature region and with the melting point of several pure chemicals (Fa. Merck) in

the high temperature region.

B-1Appendix B geothermobarometry

Appendix B Geothermobarometry

In this study several different methods were used to estimate pressures and temperatures during

UHP metamorphism and exhumation. A short description of these methods is presented below.

B1 Thermometer

B1.1 Garnet clinopyroxene thermometry

This thermometer is based on Fe, Mg exchange between garnet and clinopyroxene as defined in

the following reaction

1/3Pyrope + Hedenbergite = 1/3Almandine + Diopside

Mg3Al

2Si

3O

12 CaFeSi

2O

6 Fe

3Al

2Si

3O

12 CaMgSi

2O

6

with equilibrium constant K (Banno, 1970) defined as

(agrtFe

)1/3 (acpxMg

)K = * *

(agrtMg

)1/3 (acpxFe

)

with agrtFe

the activity of Fe in garnet, acpxMg

the activity of Mg in clinopyroxene etc. At equilibrium,

taking a standard state of pure solids at the temperature and pressure of interest ∆G°(P,T) = 0,

∆H° - T∆S° + (P-1)∆V° = -RTlnK

assuming ideal solid solution for the minerals (a = x) gives

(XGtFe

) (XCpxMg

)K = * = Kd

(XGtMg

) (XCpxFe

)

This last assumption is not completely valid and a correct treatment requires knowledge of the

mixing properties of garnet and pyroxene.

First experiments to calibrate this thermometer were made by Raheim & Green, (1974). Ellis

and Green (1979) experimentally evaluated the effect of the grossular component in garnet and

assuming that the non-ideal mixing behaviour of garnet and clinopyroxene was concentrated in XCa

of garnet proposed following empirical calibration:

3104 XGtCa

+ 3030 + 10.86 P(kb)T(K) = .

ln Kd + 1.9034 .

The same data set was used by Powell (1985) using robust regression and regression diagnostics

to give the calibration a better statistical fundament. He derived following relation:

3140 XGtCa

+ 2790 + 10 P(kb)T(K) = .

ln Kd + 1.735 .

Another calibration using this data set is Krogh’s (1988). Here the dependence of Kd on XCa

was

assumed to be curvilinear instead of linear as in the previous calibrations. He derived following

relation:

Appendix B geothermobarometryB-2

-6173(XGtCa

)2 + 6731XGtCa

+ 1879 + 10 P(kb)T(K) = .

ln Kd + 1.393 .

All these three calibrations assume an independence of Kd from the Mg number of garnet,

which was postulated by Ellis & Green (1979). A new experimental calibration of this thermometer

by Pattison & Newton, (1989), not only shows a dependence of Kd on XCa

but also on the Mg

number of garnet. Their calibration has the general form

a´X3 + b´X2 + c´X +d´T(K) = + 5.5 (P(kb)-15),

ln Kd + a0X3 + b

0X2 +c

0X4 +d

0

where the constants a´, a0, etc. depend on X

Ca in garnet (Table B1). X is the Mg number in garnet

(Mg/(Mg+Fe2+)).

The experimental data from these studies together with data from other studies were used by Ai

(1994) to propose a different calibration with a curvilinear dependence of Kd on Ca and a linear

dependence of Kd on the Mg-number of garnet. His calibration has the form:

-1629(XGtCa

)2 + 3648.55XGtCa

- 6.59 XGtMg

+ 1987.98 + 17.66 P(kb)T(K) = .

ln Kd + 1.076 .

The experimental data of Pattison & Newton (1989) were evaluated and thermodynamically

analysed by Aranovich & Pattison (1995) and Berman, Aranovich & Pattison (1995). These authors

tried to take the mixing properties of garnet and pyroxene into account and proposed a different

calibration of the garnet-clinopyroxene thermometer, that gives similar results to the Ai (1994)

calibration.

None of the calibrations takes the jadeite content of clinopyroxene into account. It was, however,

shown by Koons (1984), that jadeite contents up to Xcpx jd <0.6 do not affect temperatures calculated

with the Ellis & Green (1979) calibration.

Results calculated for all calibrations are presented in table B2. The Pattison and Newton (1989)

calibration gives consistently the lowest temperatures for the eclogites of Lago Cignana. Since the

authors suggest application of their calibration only in high grade amphibolite and eclogite facies

rock as well as in granulite facies rocks this calibration is discarded. The Ellis and Green (1979)

calibration gives always the highest temperatures and is discarded, because other studies (e.g. Green

& Adam, 1991) have shown that this calibration gives temperatures that are often 50 to 150 ° too

high. From the remaining three calibrations the Powell (1985) calibration is preferred, because it

gives an adequate description of the experimental data with a minimum number of variables.

Table B1

Parameters for the Pattison & Newton (1989) calibration of the garnet clinopyroxene thermometer.


B1.2 Amphibole-plagioclase thermometer (Holland & Blundy, 1994)

This thermometer or better these two thermometers are based on the reactions:

A) 1 edenite + 4 quartz = tremolite + albite

NaCa2Mg

5Si

4(AlSi

3)O

22(OH)

2 SiO

2 Ca

2Mg

5Si

8O

22(OH)

2NaAlSi

3O

8

B) 2 edenite + albite = richterite + anorthite

NaCa2Mg

5(AlSi

3)Si

4O

22(OH)

2 NaAlSi

3O

8 Na(CaNa)Mg

5Si

8O

22(OH)

2CaAl

2Si

2O

8

Only the thermometer based on the first reaction is discussed here, because the second reaction

requires plagioclase compositions with Xan

> 0.1, that are not found in the metabasic rocks of Lago

di Cignana.

The thermometer was calibrated using an experimental data set (Blundy & Holland, 1990), com-

bined with data from natural samples to expand the compositional relatively small range of the

experimental data set.

To use the first reaction as a thermometer, activity models for plagioclase and amphibole are

needed. For plagioclase a simplified version of the DQF (Darkens Quadratic Formalism) model

given by Holland & Powell (1992) is used. For amphibole the situation is more complicated, because

different non ideal interactions are important. Using a symmetrical form of non ideal interaction to

model the multi-site-solid-solution in amphibole and using a relative simple system involving

distribution of [ ]-K-Na-Ca-Mg-Fe2+-Fe3+-AlSi over the A, M4, M1, M2, M3 and T1 crystallographic

sites in amphibole, the number of non ideal interaction terms is reduced to 8. These 8 terms do not

have thermodynamic meaning but are a simplification useful for developing the thermometric

expression (Holland & Blundy, 1994).

The equilibrium condition for the first reaction is given by:

∆µA = 0 = ∆H°

A - T∆S°

A + P∆V°

A + RTlnK(Ed-Tr

id) + RTlnγ

ab + RTlnγ

trem - RTlnγ

ged

with KEd - Tr id = 27/256 * ((XA

[ ] * XT1

Si)/(XA

Na * XT1

Al)) * Xplag

An

and RTlnγab

= Yab

= 0 for Xab

> 0.5

and Wplag

(1-Xab

)2 + Iab

for Xab

< 0,5

Wplag

= 12 Kj, Iab

= -3,0 Kj

and Y(ed-tr)

= RTlnγed

-RTlnγtrem

= XANa

*A1 + XA

K * A

2 +XM4

Na * A

3+ XM13

Fe * A

4 + XM2

Al *A

5 +

XM2Fe

* A6 + XM2

Fe3+ *A

7 + XT1

Al * A

8 * A

9

The result is a thermometric expression for the Edenite-Tremolite thermometer:

∆H°A + P∆V°

A + Y

ab + Y

(ed-tr)T(K) = .

∆S°A - R lnK Ed - Tr

id

values for ∆H°A, ∆V°

A, ∆S°

A and for A

1 to A

9 were determined by regression of the experimental

and the natural amphibole plagioclase pairs. A9 was incorporated in ∆H°

A. A

3, A

4, A

6, A

7 and A

8

had regression values within 1 σ from zero and were removed from the regression. Following

values were determined:

Appendix B geothermobarometryB-4

∆H*(kJ) = -76.95, ∆S°(kJ K-1) = -0.065, ∆V°(kJ kbar-1) = 0.79, A1(kJ) = 39.4, A

2(kJ) = 22.4,

A5(kJ) = 41.5 - P(kbar) * 2.89. This thermometer can be used in a temperature range between 400

and 900 °C, with amphiboles that have NaA > 0.02 pfu, Alvi < 1.8 pfu and Si between 6.0 and 7.7

pfu, plagioclase must have Xan

< 0.9. Typical temperature uncertainty due to the calibration lies

around 40 °C. Results for this thermometer are presented in Table B3.

Calcite - Dolomite solvus thermometry

For this thermometer the calibration of Anovitz & Essene (1987) was used. These authors used

all available reversed experimental data on binary solvi in the system CaCO3-MgCO

3-FeCO

3 and

analyses of natural carbonates to model ternary activity/composition relationships for calcite and

dolomite structure carbonates. These data were used to model the mole fraction of MgCO3 in calcite

as a function of temperature along the calcite dolomite solvus. The least squares fit for the solvus

between 200 °C and 900 °C has the form:

TMg

(K) = A(XMgCO3

) + B/(XMgCO3

) + C(XMgCO3

)2 + D(XMgCO3

)0.5 + E

with XMgCO3

the MgCO3 concentration in Calcite. The values of the regression parameters are given

in Table B4. This thermometer and further data were used to develop a thermometer in the ternary

system CaCO3 - MgCO

3 - FeCO

3. This thermometer has the form:

TFeMg

(K) = TMg

+ a(XFeCO3

) + b(XFeCO3

)2 + c(XFeCO3

/ XMgCO3

) + d(XFeCO3

* XMgCO3

) +

e(XFeCO3

/ XMgCO3

)2 + f(XFeCO3

* XMgCO3

)2 .

with XFeCO3

and XMgCO3

respectively the FeCO3 and MgCO

3 concentrations in Calcite. The values

of the regression parameters can also be found in Table B4.

Comparison of the results of this calibration (Table B5) with results of the calibration of Powell

et al. (1984) shows no significant temperature differences.

B2 Barometer

In this study three reactions were used to estimate pressures. Two polymorphic transition reactions

that divide the P-T field in two parts were either one or the other polymorph is the stable phase. One

net transfer reaction gives a pressure estimate that depends on the composition of the reacting

phases.

The polymorphic transition reaction Coesite - Quartz gives a minimum pressure for the UHP

metamorphism. This equilibrium has been well located as a function of P and T (e.g., Mirwald &

Massonne, 1980; Bohlen & Boettcher, 1982).

Table B4

Regression parameters for the Anovitz & Essenne (1987) calibration of the calcite dolomite solvusthermometer in the system CaCO

3 - MgCO

3 and the system CaCO

3 - MgCO

3-FeCO

3 .


The polymorphic reaction Calcite-Aragonite gives a maximum pressure for the onset of lower

PT-transformation of the eclogitic mineral assemblage. This equilibrium has been well located as a

function of P and T (e.g., Johannes & Puhan, 1971; Goldsmith & Newton, 1969).

The net transfer reaction used for geobarometry is the reaction (Holland, 1980):

NaAlSi2O

6+ SiO

2= NaAlSi

3O

8

Jadeite + Quartz = Albite

The equilibrium condition for this reaction is given by

∆µ = 0 = ∆H° - T∆S° + P∆V° + RTlnK

with

aQz

* aJd

K = . a

Ab

The position of this reaction in the PT-field was calculated using the PTX-programm of Brown

et al. (1988) with the Bermann (1988) data base. Albite and quartz activities were taken as 1. The

jadeite activity in omphacite was calculated, with the method of Holland (1990) using Landau

theory to mixture according to the formula:

RT ln ajd

= RT ln (XNaM1

*XAlM2

) + RT ln γNaAl

with

RT ln γNaAl

= XCaM2

*(XMgM1

WA + X

Fe2+M1W

B + X

Fe3+M1W

C),

WA = 26 kJ, W

B = 25 kJ and W

C = 0 and with Na and Ca on the M2 site and Al, Mg, Fe2+ and Fe3+

on the M1 site. A main uncertainty factor is the ordering state of omphacite. The calculated activity

is for disordered omphacite. At the temperatures in the studied rocks between 400 and 600 °C,

omphacite should be ordered (Carpenter et al., 1990). The activity for ordered omphacites should

be lower as for disordered omphacites (Holland et al., 1990) and the pressures calculated with this

barometer (Table B6) are therefore maximum pressures only.

B-6 Appendix B Table B2 grt-cpx thermometer

GroupPositionSample

XgrtMg

XgrtCa

XgrtMg

E&GPowellKroghP&NAi

A1rBk 7

0,3230,1710,833

633607560522614

A2rBk 7

0,3540,1480,846

625599540513604

A3iBk 7

0,2580,1990,837

584559521470556

Temperaturen (°C) at 2.7 GPa

B2rBk 7

0,2930,1770,828

616591545514594

B3iBk 7

0,2560,2440,782

688665643560680

B4iBk 7

0,2760,2500,827

652629606507636

B5iBk 7

0,2290,2080,816

588563527472560

B6iBk 7

0,2880,1660,849

574547497474543

B7iBk 7

0,2690,2220,833

616592562488594

B8iBk 7

0,2690,2130,803

652627596535636

GroupPositionSample

XgrtMg

XgrtCa

XgrtMg

E&GPowellKroghP&NAi

C1rBk 7

0,2160,2620,834

587564539436558

D1rBk 7

0,3220,1770,801

685661618582678

D2iBk 7

0,2790,2380,787

704681659576700

A1rBk 8

0,3700,1410,850

628602540511607

A1rBk 39

0,2050,2680,821

595572548440567

B1rBk 39

0,2630,2390,862

580556528439551

B2iBk 39

0,1860,2510,816

570547519418539

B3iBk 39

0,1980,2170,750

635611580516616

B4alliBk 39

0,2330,2080,780

637613579529619

C1rBk 39

0,2490,2470,810

644621597507626

GroupPositionSample

XgrtMg

XgrtCa

XgrtMg

E&GPowellKroghP&NAi

C4rBk 39

0,2590,2510,872

568544517420536

C5rBk 39

0,2660,2580,844

622599575472599

C6rBk 39

0,2710,2320,842

613589560477589

D1iBk 39

0,2240,2360,797

626602575496605

D2rBk 39

0,2580,2410,817

641617592506622

A1rCig 91-1

0,3460,1350,815

658632567571644

B1iCig 90\40\2

0,1500,2310,695

632608581477613

B2iCig 90\40\2

0,2060,2410,766

645621596512627

B3iCig 90\40\2

0,1510,2270,750

579554523422550

B4iCig 90\40\2

0,1540,2230,697

631607577484611

GroupPositionSample

XgrtMg

XgrtCa

XgrtMg

E&GPowellKroghP&NAi

B5iCig 90\40\2

0,1770,2320,712

657633607523643




B-7Appendix B Table B3 amphibole-plagioclasethermometer

SampleAnalysisDate

SiO2TiO2Al2O3Cr2O3Fe2O3FeOMnOMgOCaOZnONa2OK2OTotal

H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

Bk 10 B918.10.93

52,290,085,180,032,959,170,1614,7510,750,181,620,1597,31

2,09

7,5030,4978,000

0,3790,3180,0030,0063,1551,1000,0190,0195,000

1,6530,3472,000

0,1030,0280,131

15,131

2,000

497

SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

Bk 10 B1618.10.93

51,720,026,180,023,378,160,1215,3010,930,201,930,1798,12

2,11

7,3530,6478,000

0,3880,3600,0020,0023,2420,9700,0140,0215,000

1,6650,3352,000

0,1970,0310,228

15,228

2,000

540

Bk 10 B1718.10.93

53,180,025,120,004,997,261,1515,2211,010,261,530,1599,89

2,14

7,4420,5588,000

0,2860,5260,0000,0023,1740,8490,1360,0275,000

1,6510,3492,000

0,0660,0270,093

15,093

2,000

491

Bk 10 B2018.10.93

49,600,058,460,004,799,350,1712,749,930,372,410,2698,13

2,09

7,1310,8698,000

0,5640,5180,0000,0042,7301,1240,0210,0395,000

1,5300,4702,000

0,2010,0490,250

15,250

2,000

565

Bk 10 B2118.10.93

50,500,108,080,004,948,330,0913,189,580,162,180,2297,37

2,09

7,2460,7548,000

0,6120,5340,0000,0082,8191,0000,0110,0175,000

1,4730,5272,000

0,0790,0410,120

15,120

2,000

513

Bk 10 B3318.10.93

52,090,075,490,003,336,700,0016,1210,820,701,930,1797,41

2,10

7,4210,5798,000

0,3430,3570,0000,0053,4230,7980,0000,0745,000

1,6520,3482,000

0,1850,0320,216

15,216

2,000

529

Bk 10 B3418.10.93

53,010,115,000,010,928,820,0015,9711,180,071,530,1496,76

2,10

7,5820,4188,000

0,4240,0990,0010,0083,4041,0550,0000,0075,000

1,7130,2872,000

0,1370,0260,164

15,164

2,000

489

Bk 10 B3918.10.93

53,500,114,690,222,418,230,1416,0211,210,201,460,1698,35

2,12

7,5510,4498,000

0,3320,2560,0250,0083,3700,9710,0170,0215,000

1,6950,3052,000

0,0950,0290,124

15,124

2,000

486

Bk 10 B4218.10.93

51,840,096,040,063,507,070,0915,7510,860,101,680,1997,27

2,10

7,3870,6138,000

0,4020,3750,0070,0073,3450,8430,0110,0115,000

1,6580,3422,000

0,1220,0350,158

15,158

2,000

521

Bk 10 B4718.10.93

50,450,078,470,004,018,120,0513,779,730,022,390,2597,33

2,10

7,2180,7828,000

0,6460,4320,0000,0052,9370,9720,0060,0025,000

1,4920,5082,000

0,1550,0470,201

15,201

2,000

542

Bk 10 B4918.10.93

49,790,106,990,003,318,720,0014,5311,060,001,660,3096,46

2,06

7,2300,7708,000

0,4260,3620,0000,0083,1451,0590,0000,0005,000

1,7210,2792,000

0,1880,0570,245

15,245

2,000

554

Bk 10 B5018.10.93

52,180,105,460,004,397,080,1115,7210,970,251,510,2297,99

2,11

7,4050,5958,000

0,3190,4690,0000,0083,3250,8410,0130,0265,000

1,6680,3322,000

0,0840,0410,124

15,124

2,000

505

Bk 10 B5118.10.93

50,950,068,450,005,207,210,0914,049,780,092,250,2498,36

2,12

7,2030,7978,000

0,6110,5530,0000,0052,9590,8530,0110,0095,000

1,4810,5192,000

0,0980,0440,142

15,142

2,000

529

Bk 10 B5218.10.93

50,370,086,490,004,628,970,1014,1811,080,251,580,3098,02

2,09

7,2400,7608,000

0,3390,5000,0000,0063,0381,0780,0120,0275,000

1,7060,2942,000

0,1470,0560,203

15,203

2,000

550

Bk 10 B5318.10.93

46,300,1311,180,003,5110,230,1511,9710,460,202,670,4397,23

2,05

6,7741,2268,000

0,7010,3860,0000,0102,6101,2520,0190,0225,000

1,6400,3602,000

0,3970,0820,479

15,479

2,000

594

Bk 10 B5418.10.93

50,520,036,700,044,817,460,1314,6510,820,501,710,2597,62

2,09

7,2460,7548,000

0,3780,5190,0050,0023,1320,8950,0160,0535,000

1,6630,3372,000

0,1380,0470,185

15,185

2,000

547

Bk 10 B5518.10.93

50,260,057,060,092,729,230,0814,5511,180,351,970,2997,83

2,09

7,2230,7778,000

0,4190,2940,0100,0043,1171,1090,0100,0375,000

1,7210,2792,000

0,2700,0540,325

15,325

2,000

556

Bk 10 B5718.10.93

51,240,168,230,004,817,570,0013,328,630,192,680,2297,04

2,10

7,3230,6778,000

0,7090,5170,0000,0122,8370,9040,0000,0205,000

1,3210,6792,000

0,0640,0410,105

15,105

2,000

487

Bk 10 B5818.10.93

49,810,138,330,006,076,770,0413,799,740,172,130,2397,21

2,09

7,1440,8568,000

0,5520,6550,0000,0102,9480,8120,0050,0185,000

1,4970,5032,000

0,0890,0430,132

15,132

2,000

535

Bk 10 B219.10.93

47,240,029,240,006,947,110,0013,5710,780,001,830,3797,09

2,06

6,8591,1418,000

0,4400,7580,0000,0022,9370,8630,0000,0005,000

1,6770,3232,000

0,1920,0700,262

15,262

2,000

605

Bk 10 B319.10.93

50,200,055,580,004,178,020,1515,0611,260,251,500,2796,52

2,06

7,2990,7018,000

0,2550,4570,0000,0043,2640,9760,0180,0275,000

1,7540,2462,000

0,1770,0510,228

15,228

2,000

551

Bk 10 B419.10.93

50,940,065,320,025,706,790,2415,4311,310,301,240,2397,58

2,09

7,3050,6958,000

0,2040,6160,0020,0053,2980,8140,0290,0325,000

1,7380,2622,000

0,0830,0430,126

15,126

2,000

524

norm 23 oxygen, Fe3 over Si+Ti+Al+Cr+Fe+Mg+Mn+Zn = 16


B-8 Appendix B Table B3 amphibole plagioclasethermometer

Bk 10 B1619.10.93

51,550,086,840,051,758,690,0414,7110,610,151,770,1796,41

2,08

7,4180,5828,000

0,5780,1890,0060,0063,1551,0450,0050,0165,000

1,6360,3642,000

0,1300,0320,161

15,161

2,000

511

Bk 10 B1226.11.93

51,710,135,870,043,838,250,1014,7410,630,181,620,1797,26

2,09

7,4120,5888,000

0,4040,4130,0050,0103,1490,9890,0120,0195,000

1,6330,3672,000

0,0830,0320,115

15,115

2,000

501

SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

Bk 10 B1326.11.93

49,990,146,830,024,488,560,2013,9310,650,161,730,2196,90

2,07

7,2440,7568,000

0,4110,4880,0020,0113,0091,0370,0250,0175,000

1,6540,3462,000

0,1400,0400,179

15,179

2,000

548

Bk 172725.7.94

51,720,114,230,043,1410,410,1814,2810,890,011,500,1696,68

2,06

7,5260,4748,000

0,2520,3440,0050,0123,0971,2670,0220,0015,000

1,6980,3022,000

0,1210,0300,151

15,151

2,000

507

Bk 172825.7.94

52,210,093,780,023,6010,370,2014,3010,950,001,290,1396,94

2,07

7,5740,4268,000

0,2200,3930,0020,0103,0921,2580,0250,0005,000

1,7020,2982,000

0,0650,0250,089

15,089

2,000

483

Bk 172925.7.94

52,440,073,890,014,0410,350,2714,0810,630,021,500,1397,42

2,08

7,5740,4268,000

0,2360,4390,0010,0083,0311,2500,0330,0025,000

1,6450,3552,000

0,0650,0240,090

15,090

2,000

482

Bk 173025.7.94

52,810,082,860,002,4411,290,2714,7311,670,051,010,1197,31

2,07

7,6510,3498,000

0,1390,2660,0000,0093,1811,3670,0330,0055,000

1,8110,1892,000

0,0950,0210,116

15,116

2,000

480

Bk 17513.7.94

46,910,097,810,073,8112,340,3611,8711,530,021,730,2996,83

2,02

6,9741,0268,000

0,3430,4260,0080,0102,6301,5350,0450,0025,000

1,8370,1632,000

0,3350,0560,392

15,392

2,000

577

Bk 17523.7.94

47,420,2110,630,014,379,750,1311,559,030,063,140,3096,60

2,05

6,9321,0688,000

0,7640,4800,0010,0232,5171,1920,0160,0065,000

1,4140,5862,000

0,3040,0570,362

15,362

2,000

563

Bk 17533.7.94

47,180,2010,350,014,369,610,1411,969,250,003,210,3296,59

2,05

6,9071,0938,000

0,6930,4800,0010,0222,6101,1760,0170,0005,000

1,4510,5492,000

0,3620,0610,423

15,423

2,000

559

Bk 17543.7.94

48,700,167,680,035,949,770,3012,319,720,002,470,2697,35

2,06

7,1020,8988,000

0,4220,6520,0030,0182,6761,1920,0370,0005,000

1,5190,4812,000

0,2170,0490,267

15,267

2,000

569

Bk 17553.7.94

46,870,259,160,046,0710,130,3211,019,170,122,750,3396,23

2,02

6,9481,0528,000

0,5480,6770,0050,0282,4331,2560,0400,0135,000

1,4560,5442,000

0,2470,0640,310

15,310

2,000

577

Bk 1719.7.94

52,390,051,950,003,7810,370,3515,0812,080,000,500,0796,62

2,05

7,6510,3498,000

0,0000,4160,0000,0053,2831,2660,0430,0005,013

1,8900,1102,000

0,0320,0130,045

15,058

2,000

447

Bk 1769.7.94

51,880,125,410,035,088,890,2913,629,560,122,080,1497,22

2,08

7,4720,5288,000

0,3900,5510,0030,0132,9241,0710,0350,0135,000

1,4750,5252,000

0,0560,0260,082

15,082

2,000

491

Bk 1789.7.94

51,770,124,020,055,2711,100,2112,9510,000,081,790,1797,54

2,06

7,5250,4758,000

0,2140,5770,0060,0132,8061,3500,0260,0095,000

1,5570,4432,000

0,0620,0320,094

15,094

2,000

493

Bk 1799.7.94

49,390,214,800,023,4014,190,4011,8611,610,041,260,2097,38

2,02

7,3220,6788,000

0,1600,3800,0020,0232,6211,7590,0500,0045,000

1,8440,1562,000

0,2060,0390,245

15,245

2,000

551

Bk 17109.7.94

50,820,156,730,155,299,050,2112,969,150,002,470,1697,14

2,08

7,3380,6628,000

0,4840,5750,0170,0162,7891,0930,0260,0005,000

1,4160,5842,000

0,1070,0300,137

15,137

2,000

527

Bk 17129.7.94

50,790,113,340,002,1815,280,5011,9311,830,070,880,1797,09

2,02

7,5470,4538,000

0,1320,2440,0000,0122,6421,8990,0630,0085,000

1,8830,1172,000

0,1370,0330,170

15,170

2,000

509

Bk 17419.7.94

43,530,1211,090,054,3813,540,3210,2911,700,002,270,5197,80

2,01

6,5081,4928,000

0,4620,4920,0060,0132,2931,6930,0410,0005,000

1,8740,1262,000

0,5320,0990,631

15,631

2,000

575

Bk 17429.7.94

46,450,2510,090,056,1811,220,1510,429,300,032,850,3997,38

2,04

6,8401,1608,000

0,5910,6850,0060,0282,2871,3820,0190,0035,000

1,4670,5332,000

0,2810,0750,356

15,356

2,000

581

Bk 17439.7.94

45,160,2111,600,046,7012,030,119,088,760,113,290,4697,55

2,03

6,6841,3168,000

0,7080,7460,0050,0232,0031,4900,0140,0125,000

1,3890,6112,000

0,3330,0890,422

15,422

2,000

580

Bk 17489.7.94

49,010,187,680,024,2911,210,3411,919,910,002,340,2697,15

2,05

7,1700,8308,000

0,4950,4730,0020,0202,5971,3710,0420,0005,000

1,5530,4472,000

0,2170,0500,267

15,267

2,000

555




SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

Bk 17499.7.94

47,240,159,610,014,7410,920,3111,149,360,002,900,3796,74

2,04

6,9591,0418,000

0,6270,5250,0010,0172,4461,3450,0390,0005,000

1,4770,5232,000

0,3060,0710,377

15,377

2,000

559

Bk 17509.7.94

50,600,146,680,034,3110,420,4412,539,390,002,550,1997,28

2,07

7,3410,6598,000

0,4830,4700,0030,0152,7091,2650,0540,0005,000

1,4600,5402,000

0,1770,0360,213

15,213

2,000

533

Bk 17519.7.94

50,270,167,380,024,879,390,3212,899,460,032,560,2097,55

2,08

7,2510,7498,000

0,5060,5290,0020,0172,7711,1320,0390,0035,000

1,4620,5382,000

0,1780,0380,216

15,216

2,000

547

Bk 183625.7.94

52,080,154,400,002,1512,420,2513,1410,450,001,750,1796,96

2,06

7,5920,4088,000

0,3480,2360,0000,0162,8551,5140,0310,0005,000

1,6320,3682,000

0,1270,0320,159

15,159

2,000

489

Bk 183825.7.94

51,850,163,020,052,6111,300,2414,1711,270,001,070,1095,84

2,04

7,6330,3678,000

0,1570,2890,0060,0183,1091,3910,0300,0005,000

1,7780,2222,000

0,0830,0190,102

15,102

2,000

480

Bk 185025.7.94

52,360,034,470,071,318,850,1616,1011,820,221,290,1296,80

2,08

7,5310,4698,000

0,2880,1420,0080,0033,4511,0650,0190,0235,000

1,8210,1792,000

0,1810,0220,204

15,204

2,000

510

Bk 185125.7.94

50,250,075,450,023,868,390,2314,8711,330,301,480,1596,40

2,06

7,3200,6808,000

0,2560,4230,0020,0083,2291,0220,0280,0325,000

1,7680,2322,000

0,1860,0280,215

15,215

2,000

550

Bk 185225.7.94

49,570,048,160,064,408,680,2413,159,690,322,580,2597,14

2,07

7,1700,8308,000

0,5610,4790,0070,0042,8351,0500,0290,0345,000

1,5020,4982,000

0,2250,0470,272

15,272

2,000

552

Bk 185325.7.94

51,680,065,440,074,007,980,2014,8310,390,211,820,1696,84

2,08

7,4400,5608,000

0,3630,4340,0080,0063,1820,9600,0240,0225,000

1,6030,3972,000

0,1110,0300,141

15,141

2,000

516

Bk 185525.7.94

52,850,054,970,044,057,930,2314,749,920,241,830,1396,98

2,09

7,5670,4338,000

0,4060,4360,0050,0053,1460,9490,0280,0255,000

1,5220,4782,000

0,0300,0240,054

15,054

2,000

454

Bk 185625.7.94

51,720,076,720,045,357,710,2913,388,710,262,560,1596,96

2,09

7,4230,5778,000

0,5600,5780,0050,0082,8620,9250,0350,0285,000

1,3390,6612,000

0,0520,0280,080

15,080

2,000

490

Bk 185725.7.94

52,960,055,660,032,416,720,1115,839,870,132,090,1295,98

2,10

7,5730,4278,000

0,5270,2590,0030,0053,3740,8040,0130,0145,000

1,5120,4882,000

0,0920,0220,114

15,114

2,000

480

Bk 185825.7.94

48,730,067,140,063,918,970,2213,7510,880,281,940,1896,12

2,04

7,1520,8488,000

0,3870,4310,0070,0073,0081,1020,0270,0305,000

1,7110,2892,000

0,2630,0340,297

15,297

2,000

566

Bk 3952 24.6.92

49,030,116,990,032,858,680,0914,7610,560,002,680,1995,97

2,05

7,1760,8248,000

0,3810,3140,0030,0093,2201,0620,0110,0005,000

1,6560,3442,000

0,4160,0360,453

15,453

2,000

552

Bk 3953 24.6.92

49,010,107,840,002,889,060,0813,869,630,003,180,1995,84

2,05

7,1760,8248,000

0,5290,3180,0000,0083,0251,1100,0100,0005,000

1,5110,4892,000

0,4140,0360,450

15,450

2,000

543

Bk 392513.3.93

50,530,176,630,021,088,170,0815,8310,780,112,550,2296,17

2,07

7,3120,6888,000

0,4430,1170,0020,0133,4140,9890,0100,0125,000

1,6710,3292,000

0,3870,0410,428

15,428

2,000

528

Bk 392713.3.93

51,450,086,460,023,287,470,1115,5710,250,212,670,1897,76

2,11

7,3260,6748,000

0,4100,3520,0020,0063,3040,8900,0130,0225,000

1,5640,4362,000

0,3010,0330,334

15,334

2,000

540

Bk 392813.3.93

48,340,1010,460,023,0310,050,1611,908,260,114,150,2696,83

2,06

7,0320,9688,000

0,8250,3310,0020,0082,5801,2220,0200,0125,000

1,2870,7132,000

0,4580,0490,507

15,507

2,000

540

Bk 39.143 27.8.92

48,820,058,820,024,049,710,1812,738,650,004,050,1897,25

2,07

7,0870,9138,000

0,5960,4410,0020,0042,7551,1790,0220,0005,000

1,3450,6552,000

0,4850,0340,519

15,519

2,000

541

Bk 772 6.7.92

47,980,0810,230,063,809,500,1611,447,740,003,990,1895,16

2,03

7,0780,9228,000

0,8570,4220,0070,0062,5161,1720,0200,0005,000

1,2230,7772,000

0,3650,0350,399

15,399

2,000

550

Bk 773 6.7.92

47,210,0311,720,073,4711,230,1910,247,660,004,410,2296,45

2,04

6,9331,0678,000

0,9620,3840,0080,0022,2421,3790,0240,0005,000

1,2050,7952,000

0,4610,0420,503

15,503

2,000

548

Bk 71 7.7.92

49,750,057,780,003,409,410,1612,878,550,003,430,1595,55

2,05

7,2920,7088,000

0,6360,3750,0000,0042,8121,1530,0200,0005,000

1,3430,6572,000

0,3170,0290,346

15,346

2,000

533



B-10 Appendix B Table B3 amphibole plagioclasethermometer

Bk 77 7.7.92

40,820,0715,520,003,2015,400,246,818,720,004,450,5595,78

1,96

6,2581,7428,000

1,0630,3690,0000,0061,5561,9740,0310,0005,000

1,4320,5682,000

0,7550,1100,865

15,865

2,000

665

Bk 755 7.7.92

46,900,1510,550,041,7210,490,1812,079,280,003,580,2495,20

2,02

6,9551,0458,000

0,7990,1920,0050,0122,6681,3020,0230,0005,000

1,4750,5252,000

0,5040,0460,550

15,550

2,000

545

Bk 7437.8.92

46,570,069,650,033,0510,180,1912,4410,010,203,220,2195,82

2,02

6,9061,0948,000

0,5930,3410,0040,0052,7501,2630,0240,0225,000

1,5900,4102,000

0,5160,0410,557

15,557

2,000

565

Bk 7477.8.92

47,260,049,510,003,379,640,2112,8610,100,153,100,2096,44

2,04

6,9391,0618,000

0,5840,3720,0000,0032,8141,1840,0260,0165,000

1,5890,4112,000

0,4710,0380,510

15,510

2,000

569

Bk 7487.8.92

52,240,014,930,061,496,940,1517,0311,310,231,930,0896,40

2,09

7,4870,5138,000

0,3200,1610,0070,0013,6380,8320,0180,0245,000

1,7370,2632,000

0,2730,0150,288

15,288

2,000

519

Bk 7497.8.92

51,520,077,560,014,846,640,2214,028,270,243,260,1496,80

2,10

7,3650,6358,000

0,6390,5210,0010,0052,9870,7940,0270,0255,000

1,2670,7332,000

0,1700,0260,196

15,196

2,000

525

Bk 81514.3.93

49,980,158,950,083,048,070,1213,809,200,163,190,2496,98

2,09

7,1790,8218,000

0,6950,3290,0090,0122,9550,9700,0150,0175,000

1,4160,5842,000

0,3040,0450,349

15,349

2,000

548

Bk 81714.3.93

51,230,036,460,000,628,830,1115,5310,700,192,520,1696,37

2,08

7,3930,6078,000

0,4920,0670,0000,0023,3401,0650,0130,0205,000

1,6540,3462,000

0,3590,0300,390

15,390

2,000

516

Bk 81814.3.93

48,240,0510,670,002,868,180,1013,269,370,233,380,2696,60

2,07

6,9801,0208,000

0,7990,3110,0000,0042,8600,9890,0120,0255,000

1,4530,5472,000

0,4010,0490,450

15,450

2,000

560

Bk 81914.3.93

52,130,054,870,001,716,670,1117,1711,570,171,550,1696,16

2,09

7,4820,5188,000

0,3060,1840,0000,0043,6730,8010,0130,0185,000

1,7790,2212,000

0,2110,0300,241

15,241

2,000

521

Bk 9623.2.94

52,040,124,990,040,879,150,0515,6211,430,191,390,1396,02

2,07

7,5350,4658,000

0,3860,0950,0050,0093,3711,1080,0060,0205,000

1,7730,2272,000

0,1630,0250,188

15,188

2,000

505

SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

Bk 9823.2.94

51,450,086,810,001,978,110,1114,7410,050,142,150,1495,75

2,07

7,4360,5648,000

0,5960,2140,0000,0063,1750,9800,0130,0155,000

1,5560,4442,000

0,1590,0260,185

15,185

2,000

513

Bk 91223.2.94

53,630,054,350,040,089,280,0816,2511,490,111,420,0896,86

2,10

7,6610,3398,000

0,3930,0080,0050,0043,4601,1090,0100,0125,000

1,7590,2412,000

0,1520,0150,167

15,167

2,000

476

Bk 91323.2.94

50,360,128,090,031,788,800,1213,9510,030,232,370,1896,06

2,07

7,2950,7058,000

0,6760,1940,0030,0093,0121,0660,0150,0255,000

1,5570,4432,000

0,2220,0340,256

15,256

2,000

536

Bk 92023.2.94

45,270,1511,040,054,4510,600,1711,0410,020,122,770,2895,96

2,01

6,7411,2598,000

0,6790,4980,0060,0122,4501,3200,0210,0135,000

1,5990,4012,000

0,3980,0540,453

15,453

2,000

604

Bk 91424.2.94

47,260,3010,260,013,2610,010,0912,039,720,072,810,2696,09

2,04

6,9491,0518,000

0,7270,3610,0010,0242,6361,2310,0110,0085,000

1,5310,4692,000

0,3320,0500,382

15,382

2,000

579

Bk 91524.2.94

48,160,289,900,043,269,960,1411,799,040,173,030,2395,99

2,04

7,0660,9348,000

0,7770,3600,0050,0222,5781,2220,0170,0185,000

1,4210,5792,000

0,2830,0440,327

15,327

2,000

564

Bk 91624.2.94

48,380,408,340,103,309,700,1212,9010,250,182,270,2396,17

2,04

7,1020,8988,000

0,5450,3650,0120,0322,8221,1910,0150,0205,000

1,6120,3882,000

0,2580,0440,302

15,302

2,000

572

Bk 92524.2.94

45,990,2210,270,003,4411,090,1411,4610,160,162,780,2995,99

2,02

6,8411,1598,000

0,6420,3850,0000,0182,5411,3790,0180,0185,000

1,6190,3812,000

0,4210,0560,477

15,477

2,000

587

Bk 92624.2.94

46,740,049,890,023,3010,470,1112,0410,180,102,680,2895,85

2,02

6,9221,0788,000

0,6480,3680,0020,0032,6571,2970,0140,0115,000

1,6150,3852,000

0,3850,0540,439

15,439

2,000

580

Bk 92724.2.94

49,400,008,100,062,737,980,0514,5610,570,112,310,1496,00

2,07

7,1720,8288,000

0,5580,2980,0070,0003,1510,9690,0060,0125,000

1,6440,3562,000

0,2940,0260,321

15,321

2,000

561

Bk 92924.2.94

49,440,148,460,001,719,580,0713,459,990,122,540,2195,71

2,05

7,2230,7778,000

0,6800,1880,0000,0112,9291,1710,0090,0135,000

1,5640,4362,000

0,2830,0400,323

15,323

2,000

544




SampleAnalysisDate


H2O

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

T in °C

Bk 9224.3.94

48,770,149,260,053,7010,280,1512,309,960,202,600,2597,66

2,07

7,0610,9398,000

0,6410,4030,0060,0112,6541,2450,0180,0215,000

1,5450,4552,000

0,2750,0470,322

15,322

2,000

572

Bk 9234.3.94

48,770,178,580,002,8510,570,1512,6710,270,162,450,2596,90

2,05

7,1160,8848,000

0,5920,3130,0000,0132,7561,2900,0190,0175,000

1,6060,3942,000

0,2990,0480,346

15,346

2,000

564

Cig 91-17317.6.93

47,670,288,820,000,989,380,0915,0511,680,002,660,3396,94

2,06

6,9391,0618,000

0,4530,1080,0000,0223,2651,1410,0110,0005,000

1,8220,1782,000

0,5720,0630,635

15,635

2,000

556

Cig 91-17417.6.93

45,180,2612,610,021,6310,110,1212,4010,240,003,550,4096,51

2,04

6,6401,3608,000

0,8240,1800,0020,0212,7161,2420,0150,0005,000

1,6120,3882,000

0,6240,0770,701

15,701

2,000

574


B-12 Appendix B Table B5 calcite-dolomite solvusthermometer

sampleanalysisdateCL colour

CaOMgOFeOMnO

Sum

CO2

total

CaMgFeMn

CO3

T(Mg)°CT(Fe,Mg)°C

Bk 7726.4.93yellow

52,391,972,130,65

57,14

44,97

102,11

0,9140,0480,0290,009

1,000

518538

Bk 7826.4.93brown

50,902,552,410,65

56,51

44,61

101,12

0,8950,0620,0330,009

1,000

572577

Bk 72126.4.93yellow

51,102,392,190,56

56,24

44,40

100,64

0,9030,0590,0300,008

1,000

560568

Bk 72226.4.93yellow

50,552,432,450,53

55,96

44,15

100,11

0,8980,0600,0340,007

1,000

564571

Bk 76326.4.93yellow

53,281,311,470,63

56,69

44,53

101,22

0,9390,0320,0200,009

1,000

442470

Bk 76426.4.93yellow

51,921,301,570,57

55,36

43,48

98,84

0,9370,0330,0220,008

1,000

445475

Bk 726.7.92yellow

63,611,241,400,86

67,11

52,66

119,77

0,9480,0260,0160,010

1,000

400429

Bk 746.7.92yellow

62,281,682,111,06

67,13

52,66

119,79

0,9280,0350,0250,012

1,000

457488

Bk 7106.7.92orange

59,982,182,721,29

66,17

51,92

118,09

0,9070,0460,0320,015

1,000

510533

Bk 7336.7.92yellow

62,601,011,871,07

66,55

52,04

118,59

0,9440,0210,0220,013

1,000

362407

Bk 7Th311.6.94yellow

54,901,851,200,64

58,59

46,24

104,83

0,9320,0440,0160,009

1,000

501516


54,281,771,540,68

58,27

45,90

104,17

0,9280,0420,0210,009

1,000

494513


CaOMgOFeOMnO

Sum

CO2

total

CaMgFeMn

CO3

T(Mg)°CT(Fe,Mg)°C

Bk 7Th711.6.94orange

53,651,971,850,73

58,20

45,84

104,04

0,9180,0470,0250,010

1,000

515533


51,421,751,430,50

55,10

43,45

98,55

0,9290,0440,0200,007

1,000

502520


51,381,832,120,96

56,29

44,21

100,50

0,9120,0450,0290,013

1,000

507530


52,791,962,520,82

58,09

45,62

103,71

0,9080,0470,0340,011

1,000

515537


51,541,301,770,72

55,33

43,40

98,73

0,9320,0330,0250,010

1,000

446479


52,911,261,730,71

56,61

44,40

101,01

0,9350,0310,0240,010

1,000

435469


49,871,661,960,74

54,23

42,61

96,84

0,9190,0430,0280,011

1,000

496520


50,591,621,900,68

54,79

43,06

97,85

0,9220,0410,0270,010

1,000

489514


50,051,701,800,69

54,24

42,66

96,90

0,9210,0440,0260,010

1,000

500522


50,211,411,790,54

53,95

42,37

96,32

0,9300,0360,0260,008

1,000

465495


49,401,691,980,74

53,81

42,29

96,10

0,9170,0440,0290,011

1,000

501524


51,131,341,570,59

54,63

42,92

97,55

0,9350,0340,0220,009

1,000

453482


49,921,762,270,62

54,57

42,87

97,44

0,9140,0450,0320,009

1,000

506530


50,641,711,940,70

54,99

43,23

98,22

0,9190,0430,0270,010

1,000

499522


50,641,752,130,67

55,19

43,37

98,56

0,9160,0440,0300,010

1,000

502526


50,921,381,970,60

54,87

43,05

97,92

0,9280,0350,0280,009

1,000

458492


50,631,502,020,46

54,61

42,89

97,50

0,9260,0380,0290,007

1,000

475505


52,621,051,600,55

55,82

43,76

99,58

0,9440,0260,0220,008

1,000

403441


50,631,502,020,46

54,61

42,89

97,50

0,9260,0380,0290,007

1,000

475505


52,621,051,600,55

55,82

43,76

99,58

0,9440,0260,0220,008

1,000

403441

Bk 7Th3611.6.94brown

50,981,601,940,70

55,22

43,38

98,60

0,9220,0400,0270,010

1,000

485512


CaOMgOFeOMnO

Sum

CO2

total

CaMgFeMn

CO3

T(Mg)°CT(Fe,Mg)°C

B-13Appendix B Table B5 calcite-dolomite solvusthermometer


CaOMgOFeOMnO

Sum

CO2

total

CaMgFeMn

CO3

T(Mg)°CT(Fe,Mg)°C


CaOMgOFeOMnO

Sum

CO2

total

CaMgFeMn

CO3

T(Mg)°CT(Fe,Mg)°C


50,371,641,790,66

54,46

42,83

97,29

0,9230,0420,0260,010

1,000

492516


50,521,601,930,60

54,65

42,95

97,60

0,9230,0410,0280,009

1,000

487513


51,271,511,690,68

55,15

43,34

98,49

0,9280,0380,0240,010

1,000

474500


53,030,720,750,69

55,19

43,29

98,48

0,9610,0180,0110,010

1,000

329355


52,140,980,970,65

54,74

42,99

97,73

0,9520,0250,0140,009

1,000

393419


53,130,710,730,62

55,19

43,30

98,49

0,9630,0180,0100,009

1,000

326352


51,721,330,930,55

54,53

42,95

97,48

0,9450,0340,0130,008

1,000

452470


52,471,220,980,75

55,42

43,58

99,00

0,9450,0310,0140,011

1,000

433454


52,241,431,460,64

55,77

43,85

99,62

0,9350,0360,0200,009

1,000

462487


51,581,411,190,52

54,70

43,07

97,77

0,9400,0360,0170,007

1,000

462484


52,051,401,160,64

55,25

43,48

98,73

0,9390,0350,0160,009

1,000

459480


52,241,000,870,58

54,69

42,98

97,67

0,9540,0250,0120,008

1,000

397420


53,380,720,920,56

55,58

43,59

99,17

0,9610,0180,0130,008

1,000

328359


51,471,601,450,70

55,22

43,46

98,68

0,9290,0400,0200,010

1,000

485506


51,191,521,290,71

54,71

43,06

97,77

0,9330,0390,0180,010

1,000

477497

B-14 Appendix B Table B6 jadeite-quartz-albitebarometer

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 391,34.5.92

1,9950,0052,000

0,4740,0330,0010,509

0,4310,0830,0000,4740,5030,0011,491

2,000

823

1,30

Bk 399,24.5.92

1,9980,0022,000

0,4450,0290,0010,475

0,4560,0800,0010,5130,4740,0001,525

2,000

823

1,30

Bk 3910,24.5.92

2,002-0,0022,000

0,4520,0240,0010,477

0,4510,0880,0000,5030,4800,0001,523

2,000

823

1,30

Bk 3912,24.5.92

1,9990,0012,000

0,4320,0410,0010,473

0,4510,0910,0000,5120,4720,0011,527

2,000

823

1,28

Bk 3913,24.5.92

1,9880,0122,000

0,4640,0660,0010,530

0,4200,0570,0010,4730,5190,0001,470

2,000

823

1,27

Bk 3914,24.5.92

1,9930,0072,000

0,4290,0650,0010,496

0,4420,0690,0010,5020,4890,0001,504

2,000

823

1,27

Bk 39823.3.92

1,9730,0272,000

0,4350,1560,0000,591

0,3850,0160,0000,4430,5640,0001,409

2,000

823

1,21

Bk 39923.3.92

1,9360,0642,000

0,4470,0560,0010,504

0,4310,2690,0030,3520,4390,0031,496

2,000

823

1,26

BK 391023.3.92

1,9450,0552,000

0,4260,0550,0010,482

0,4400,1770,0020,4720,4260,0011,518

2,000

823

1,27

BK 392,34.5.92

1,9970,0032,000

0,4810,0390,0000,521

0,4130,0760,0010,4710,5180,0001,479

2,000

823

1,29

Bk 391,15.5.92

1,9890,0112,000

0,4670,0770,0010,545

0,3680,1100,0010,4400,5340,0011,455

2,000

823

1,27

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 392,15.5.92

1,9930,0072,000

0,4500,0570,0010,508

0,4250,0740,0020,4900,5020,0001,492

2,000

823

1,28

Bk 393,25.5.92

1,9980,0022,000

0,4600,0740,0010,536

0,3900,0840,0000,4550,5350,0001,464

2,000

823

1,27

Bk 394,25.5.92

2,001-0,0012,000

0,4630,0570,0010,523

0,3870,0930,0000,4720,5250,0001,477

2,000

823

1,28

Bk 395,15.5.92

1,9970,0032,000

0,4680,0680,0010,538

0,3930,0720,0000,4610,5350,0001,462

2,000

823

1,27

Bk 396,15.5.92

1,9950,0052,000

0,4790,0660,0010,546

0,3850,0780,0000,4500,5410,0001,454

2,000

823

1,28

Bk 398,15.5.92

2,002-0,0022,000

0,5310,0780,0010,611

0,3060,0930,0000,3750,6130,0011,389

2,000

823

1,28

Bk 3910,15.5.92

1,9870,0132,000

0,4690,0700,0010,539

0,4060,0970,0000,4300,5260,0011,461

2,000

823

1,27

Bk 3911,15.5.92

1,9920,0082,000

0,4640,0940,0010,559

0,3770,0690,0010,4430,5510,0001,441

2,000

823

1,26

Bk 39124.6.92

1,9900,0102,000

0,4930,1020,0000,596

0,3420,0760,0020,3980,5860,0001,404

2,000

823

1,26

Bk 39324.6.92

2,012-0,0122,000

0,4900,0210,0010,513

0,3950,1340,0020,4300,5260,0001,487

2,000

823

1,30

Bk 39424.6.92

1,9850,0152,000

0,4700,0730,0010,545

0,3890,0830,0000,4520,5300,0001,455

2,000

823

1,27

Bk 393824.6.92

1,9970,0032,000

0,4120,0620,0010,476

0,4250,1100,0000,5150,4740,0001,524

2,000

823

1,27

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 396124.6.92

2,0000,0002,000

0,4790,0290,0010,511

0,4140,0930,0000,4720,5110,0001,489

2,000

823

1,30

Bk 39428.8.92

1,9880,0122,000

0,4710,0860,0010,557

0,3810,0760,0010,4390,5450,0001,443

2,000

823

1,26

Bk 39528.8.92

1,9770,0232,000

0,4510,1230,0010,576

0,3830,0400,0000,4450,5530,0011,424

2,000

823

1,24

Bk 391028.8.92

1,9910,0092,000

0,4520,1020,0010,555

0,3850,0610,0000,4490,5460,0001,445

2,000

823

1,25

Bk 391128.8.92

1,9760,0242,000

0,4280,1730,0010,603

0,3260,0740,0000,4160,5800,0001,397

2,000

823

1,20

Bk 391328.8.92

1,9950,0052,000

0,4650,0810,0030,549

0,3780,0910,0010,4330,5470,0001,451

2,000

823

1,26

Bk 391428.8.92

1,9890,0112,000

0,4610,0670,0010,530

0,3870,0910,0000,4720,5190,0001,470

2,000

823

1,27

Bk 392928.8.92

1,9850,0152,000

0,4650,0580,0010,525

0,4110,0800,0010,4720,5100,0001,475

2,000

823

1,28

Bk 3930 28.8.92

1,9880,0122,000

0,4420,0480,0000,490

0,4560,0610,0010,5140,4780,0001,510

2,000

823

1,28

Bk 393128.8.92

1,9850,0152,000

0,4470,0580,0010,507

0,4520,0460,0000,5010,4910,0011,493

2,000

823

1,28

B-15Appendix B Table B6 jadeite-quartz-albitebarometer

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 393228.8.92

1,9820,0182,000

0,4440,0630,0010,507

0,4470,0560,0000,5010,4890,0011,493

2,000

823

1,27

Bk 393328.8.92

1,9770,0232,000

0,3880,0720,0010,461

0,5020,0430,0010,5530,4380,0001,539

2,000

823

1,25

Bk 393428.8.92

1,9810,0192,000

0,4440,0690,0020,515

0,4480,0380,0000,5010,4960,0011,485

2,000

823

1,27

Bk 393528.8.92

1,9840,0162,000

0,4450,0510,0010,496

0,4580,0520,0000,5120,4810,0011,504

2,000

823

1,28

Bk 393628.8.92

1,9850,0152,000

0,4290,0620,0010,493

0,4600,0480,0010,5190,4790,0001,507

2,000

823

1,27

Bk 393728.8.92

1,9820,0182,000

0,3950,0980,0000,495

0,4460,0650,0020,5110,4770,0011,505

2,000

823

1,24

Bk 393928.8.92

1,9900,0102,000

0,3950,0730,0010,469

0,4510,0870,0000,5330,4590,0011,531

2,000

823

1,25

Bk 394028.8.92

1,9900,0102,000

0,4570,0430,0000,500

0,4420,0630,0020,5010,4900,0011,500

2,000

823

1,29

Bk 394128.8.92

1,9880,0122,000

0,4700,0410,0010,513

0,4370,0640,0020,4830,5020,0001,487

2,000

823

1,29

Bk 394228.8.92

1,9880,0122,000

0,4590,0420,0010,503

0,4430,0670,0010,4930,4900,0011,497

2,000

823

1,29

Bk 395328.8.92

1,9790,0212,000

0,3850,1260,0010,512

0,4060,0870,0020,4980,4890,0021,488

2,000

823

1,21

Bk 395428.8.92

1,9770,0232,000

0,3910,1180,0010,510

0,3980,0880,0030,5130,4860,0011,490

2,000

823

1,22

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 395528.8.92

1,9690,0312,000

0,3930,1120,0010,506

0,4160,0880,0020,5100,4740,0021,494

2,000

823

1,22

Bk 395528.1.93

1,9730,0272,000

0,4210,1390,0010,563

0,3880,0500,0110,4480,5350,0011,437

2,000

823

1,22

Bk 395728.1.93

1,9950,0052,000

0,4610,0650,0010,527

0,3950,0860,0010,4650,5220,0001,473

2,000

823

1,27

Bk 396028.1.93

1,9820,0182,000

0,4360,0830,0010,521

0,4300,0570,0010,4790,4980,0051,479

2,000

823

1,26

Bk 73825.6.92

1,9860,0142,000

0,4140,0700,0010,486

0,4260,0850,0020,5280,4730,0001,514

2,000

823

1,26

Bk 7126.7.92

1,9950,0052,000

0,4620,0760,0010,540

0,3770,0870,0010,4580,5370,0001,460

2,000

823

1,27

Bk 7236.7.92

1,9940,0062,000

0,4940,0620,0010,556

0,3800,0690,0010,4440,5490,0011,444

2,000

823

1,28

Bk 7556.7.92

1,9860,0142,000

0,4170,1080,0010,528

0,3870,0950,0040,4700,5150,0001,472

2,000

823

1,24

Bk 7686.7.92

1,9780,0222,000

0,4200,1010,0010,523

0,3980,0830,0000,4940,5020,0001,477

2,000

823

1,24

Bk 7746.7.92

1,9990,0012,000

0,4510,0510,0000,503

0,4080,0970,0010,4870,5030,0001,497

2,000

823

1,28

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 737.7.92

1,9940,0062,000

0,4530,0480,0010,503

0,3980,1020,0000,4980,4980,0001,497

2,000

823

1,28

Bk 747.7.92

1,9870,0132,000

0,4340,0620,0000,496

0,4120,0840,0020,5220,4830,0011,504

2,000

823

1,27

Bk 767.7.92

1,9810,0192,000

0,4310,0800,0000,512

0,4110,0720,0020,5090,4940,0001,488

2,000

823

1,26

Bk 7427.7.92

1,9950,0052,000

0,5180,0560,0010,576

0,3570,0740,0010,4210,5710,0001,424

2,000

823

1,29

Bk 7457.7.92

1,9810,0192,000

0,4330,0920,0010,526

0,3970,0650,0000,5060,5070,0001,474

2,000

823

1,25

Bk 7467.7.92

1,9780,0222,000

0,4610,0660,0010,530

0,3910,1130,0030,4540,5080,0011,470

2,000

823

1,27

Bk 7507.7.92

1,9770,0232,000

0,4330,0910,0010,525

0,4010,0590,0030,5090,5020,0001,475

2,000

823

1,25

Bk 7577.7.92

2,006-0,0062,000

0,4520,0390,0010,494

0,4070,1200,0030,4760,5000,0001,506

2,000

823

1,29

Bk 71527.8.92

1,9770,0232,000

0,4250,0900,0010,518

0,4130,0600,0020,5080,4940,0011,482

2,000

823

1,25

Bk 71727.8.92

1,9770,0232,000

0,4290,0830,0010,515

0,4090,0660,0010,5090,4930,0001,485

2,000

823

1,25

Bk 71827.8.92

1,9930,0072,000

0,4410,0340,0010,476

0,4060,1190,0020,5170,4690,0001,524

2,000

823

1,29

B-16 Appendix B Table B6 jadeite-quartz-albitebarometer

Bk 81229.1.93b

1,9950,0052,000

0,5650,0180,0020,586

0,3430,0870,0010,3920,5810,0011,414

2,000

823

1,32

Bk 72827.8.92

1,9890,0112,000

0,4490,0270,0000,478

0,4340,0940,0020,5220,4670,0001,522

2,000

823

1,30

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 73027.8.92

1,9750,0252,000

0,3800,0720,0000,455

0,4770,0560,0020,5710,4310,0001,545

2,000

823

1,25

Bk 73527.8.92

1,9800,0202,000

0,4450,0550,0010,503

0,4270,0720,0010,5100,4820,0011,497

2,000

823

1,28

Bk 73727.8.92

1,9750,0252,000

0,3830,0770,0000,462

0,4580,0650,0010,5710,4360,0011,538

2,000

823

1,25

Bk 74127.8.92

1,9650,0352,000

0,3660,1070,0000,473

0,4860,0250,0020,5690,4370,0011,527

2,000

823

1,22

Bk 74227.8.92

1,9810,0192,000

0,4040,0510,0010,456

0,4620,0780,0020,5600,4350,0011,544

2,000

823

1,27

Bk 75127.8.92

1,9800,0202,000

0,4490,0750,0000,524

0,4050,0660,0020,4930,5030,0011,476

2,000

823

1,26

Bk 75327.8.92

1,9840,0162,000

0,4280,0630,0010,491

0,4110,0920,0010,5230,4760,0001,509

2,000

823

1,27

Bk 81414.3.93

1,9850,0152,000

0,5380,0650,0010,605

0,3580,0430,0010,3960,5640,0261,395

2,000

823

1,28

Bk 83614.3.93

1,9840,0162,000

0,4570,0610,0010,519

0,4010,0710,0020,5000,5030,0011,481

2,000

823

1,27

Bk 83714.3.93

1,9830,0172,000

0,4680,0600,0010,529

0,3990,0730,0000,4810,5110,0011,471

2,000

823

1,28

Bk 83814.3.93

1,9920,0082,000

0,4390,0270,0020,468

0,4350,1070,0020,5220,4620,0001,532

2,000

823

1,30

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Bk 83914.3.93

1,9950,0052,000

0,4570,0240,0000,481

0,4230,1020,0020,5090,4760,0011,519

2,000

823

1,30

Bk 84214.3.93

1,9920,0082,000

0,4380,0660,0000,504

0,4050,0890,0020,5000,4960,0011,496

2,000

823

1,27

Bk 84314.3.93

1,9950,0052,000

0,4530,0490,0010,504

0,3810,1100,0020,4960,4990,0011,496

2,000

823

1,28

Bk 8329.1.93a

1,9910,0092,000

0,5130,0160,0080,538

0,4030,0820,0000,4290,5290,0071,462

2,000

823

1,31

Bk 8429.1.93a

2,0000,0002,000

0,5120,0040,0060,523

0,3970,1100,0020,4360,5280,0011,477

2,000

823

1,32

Bk 8529.1.93a

1,9970,0032,000

0,4870,0140,0040,505

0,3850,1250,0070,4680,5060,0001,495

2,000

823

1,31

Bk 81429.1.93a

1,9800,0202,000

0,4520,0630,0010,516

0,4130,0730,0020,4950,4960,0011,484

2,000

823

1,27

Bk 82029.1.93a

1,9860,0142,000

0,5560,0600,0010,618

0,3410,0540,0010,3760,6040,0011,382

2,000

823

1,29

Bk 82129.1.93a

1,9920,0082,000

0,4750,0790,0000,555

0,3810,0810,0010,4330,5470,0011,445

2,000

823

1,27

Bk 82329.1.93a

1,9830,0172,000

0,4700,0530,0000,523

0,4050,0790,0010,4800,5050,0021,477

2,000

823

1,28

sampleanalysisdate

SiAlt

AloFe3Ti

MgFe2MnCaNaK

sum

at T (K)

P (Gpa)

Cig90/40/2456.1.91

2,0030,0002,003

0,5020,0480,0010,550

0,3680,1030,0010,4180,5570,0001,447

1,997

823

1,29

Cig90\40\133?

1,9980,0022,000

0,5070,0600,0010,568

0,3620,0860,0000,4170,5670,0001,432

2,000

823

1,28

Cig90\40\148?

2,0030,0002,003

0,5110,0430,0010,555

0,3690,0920,0000,4190,5630,0001,441

1,997

823

1,30

Cig90\40\165?

1,9930,0072,000

0,4290,0830,0010,513

0,3620,1360,0000,4820,5070,0001,487

2,000

823

1,25

Cig90\40\166?

1,9810,0192,000

0,4710,1110,0010,583

0,3760,0400,0000,4340,5650,0001,417

2,000

823

1,25

Cig90\40\167?

1,9950,0052,000

0,4790,0760,0010,556

0,3760,0810,0000,4360,5520,0001,444

2,000

823

1,27

Cig90\40\168?

2,0000,0002,000

0,4650,0750,0000,540

0,3830,0880,0000,4490,5400,0001,460

2,000

823

1,27

C-1Appendix C

Table C1

List of samples, XRD is powder X-ray diffraction, EMP is electron microprobe, CL is cathodoluminescence,SEM is scanning electron microscopy, XRF is X-ray fluorescence spectroscopy, UST is universal stage, IAis image analysis, FIS is microthermometry

C-2 Appendix C

Table C1 continued


C-3Appendix C

Table C1 continued


C-4 Appendix C

Table C1 continued


C-5Appendix C

Table C2

Whole rock analyses fpr major and trace elementsfrom samples of group 1 to 4 eclogites

C-6 Appendix C Table C3 omphacite

normed to 4 cations, Fe3 over charge balance (12+)


position means analysis of: i(x), inclusion of cpx in mineral x, core is core position in a cpx grain, mineral x, rimposition in cpx grain in contact with mineral x, mineral x(i), cpx at an inclusion of mineral x in cpx

sampleanalysisdateposition

SiO2TiO2Al2O3Cr2O3Fe2O3FeOMnOMgOCaOZnONa2OK2Ototal

SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 398,213.3.93i (gnt)

55,790,0410,800,036,552,310,025,9710,630,158,610,03100,93

1,9820,0182,000

0,4350,1750,0010,0010,611

0,3160,0690,0010,4050,0040,5930,0011,389

4,000

Bk 399,213.3.93i (gnt)

55,850,0610,750,135,372,640,076,3011,050,178,320,00100,71

1,9870,0132,000

0,4370,1440,0040,0010,586

0,3340,0780,0020,4210,0040,5740,0001,414

4,000

Bk 39623.3.92i (gnt)

55,550,0312,360,053,722,320,035,909,98n.a8,790,0198,74

1,9930,0072,000

0,5160,1000,0010,0010,618

0,3160,0700,0010,384-0,6110,0001,382

4,000

Bk 39723.3.92i (gnt)

55,880,0312,670,002,243,240,045,909,82n.a8,720,0198,54

2,0050,0002,005

0,5410,0600,0000,0010,602

0,3160,0970,0010,377-0,6070,0001,398

4,000

Bk 39823.3.92i (gnt)

54,930,0010,900,005,780,540,017,1911,50n.a8,100,0198,96

1,9730,0272,000

0,4350,1560,0000,0000,591

0,3850,0160,0000,443-0,5640,0001,409

4,000

Bk 391223.3.92core

55,120,0410,460,045,031,120,027,2811,58n.a7,970,0198,66

1,9870,0132,000

0,4310,1360,0010,0010,570

0,3910,0340,0010,447-0,5570,0001,430

4,000

Bk 391323.3.92core

55,560,0210,670,002,841,190,038,4013,13n.a7,210,0099,05

1,9870,0132,000

0,4360,0760,0000,0000,513

0,4480,0360,0010,503-0,5000,0001,487

4,000

Bk 391723.3.92i (gnt)

55,200,0311,970,043,872,580,006,1010,33n.a8,470,0298,61

1,9890,0112,000

0,4970,1050,0010,0010,603

0,3280,0780,0000,399-0,5920,0011,397

4,000

Bk 391923.3.92core

55,190,0210,840,034,531,580,007,1511,58n.a7,940,0198,87

1,9850,0152,000

0,4450,1230,0010,0000,569

0,3830,0480,0000,446-0,5540,0001,431

4,000

Bk 392023.3.92core

55,350,0510,340,022,401,590,028,5713,40n.a6,930,0198,68

1,9890,0112,000

0,4270,0650,0010,0010,493

0,4590,0480,0010,516-0,4830,0001,507

4,000

Bk 39124.6.92gnt

55,210,0211,850,003,782,520,066,3610,31n.a8,390,0098,50

1,9900,0102,000

0,4930,1020,0000,0000,596

0,3420,0760,0020,398-0,5860,0001,404

4,000

Bk 39424.6.92i (gnt)

55,230,0511,460,032,682,770,017,2611,74n.a7,610,0198,85

1,9850,0152,000

0,4700,0730,0010,0010,545

0,3890,0830,0000,452-0,5300,0001,455

4,000

Bk 391524.6.92i (gnt)

54,860,0510,560,063,503,490,086,5111,55n.a7,690,0098,35

1,9950,0052,000

0,4480,0960,0020,0010,546

0,3530,1060,0020,450-0,5420,0001,454

4,000

Bk 391624.6.92i (gnt)

54,570,0010,670,033,733,530,106,5111,64n.a7,570,0098,35

1,9870,0132,000

0,4450,1020,0010,0000,548

0,3530,1080,0030,454-0,5340,0001,452

4,000

Bk 393824.6.92cpx

54,850,049,670,042,263,610,017,8313,21n.a6,710,0098,23

1,9970,0032,000

0,4120,0620,0010,0010,476

0,4250,1100,0000,515-0,4740,0001,524

4,000

Bk 396124.6.92gnt

55,700,0511,330,051,073,090,007,7312,26n.a7,340,0198,63

2,0000,0002,000

0,4790,0290,0010,0010,511

0,4140,0930,0000,472-0,5110,0001,489

4,000

Bk 391128.1.93i (gnt)

55,290,0110,580,054,003,260,066,8411,870,207,590,0199,76

1,9860,0142,000

0,4330,1080,0010,0000,543

0,3660,0980,0020,4570,0050,5280,0001,457

4,000

Bk 391328.1.93i (gnt)

55,180,0711,300,052,235,040,026,0310,350,007,970,0098,24

2,0060,0002,006

0,4900,0610,0010,0010,554

0,3270,1530,0010,4030,0000,5620,0001,446

4,000

Bk 391428.1.93i (gnt)

55,150,0611,500,083,982,910,026,2910,870,138,140,0299,15

1,9840,0162,000

0,4720,1080,0020,0010,583

0,3370,0870,0010,4190,0030,5680,0011,417

4,000

Bk 391528.1.93i (gnt)

55,070,0711,240,056,013,310,045,249,560,218,780,0299,60

1,9850,0152,000

0,4620,1630,0010,0010,628

0,2820,1000,0010,3690,0060,6140,0011,372

4,000

Bk 391628.1.93i (gnt)

54,600,039,820,067,073,160,035,6510,580,328,220,0399,57

1,9820,0182,000

0,4020,1930,0020,0010,597

0,3060,0960,0010,4110,0090,5790,0011,403

4,000

Bk 391728.1.93i (gnt)

54,210,059,330,026,474,640,065,3910,600,137,940,0198,86

1,9900,0102,000

0,3940,1790,0010,0010,574

0,2950,1430,0020,4170,0040,5650,0001,426

4,000

C-7Appendix C Table C3 omphacite




Bk 39428.8.92cpx

55,370,0311,420,003,192,530,027,1311,420,007,830,0198,95

1,9880,0122,000

0,4710,0860,0000,0010,557

0,3810,0760,0010,4390,0000,5450,0001,443

4,000



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 39528.8.92cpx

54,850,0611,160,034,521,330,017,1311,530,047,910,0398,60

1,9770,0232,000

0,4510,1230,0010,0010,576

0,3830,0400,0000,4450,0010,5530,0011,424

4,000

Bk 39628.8.92coes (i)

55,430,0310,970,031,961,760,048,4413,160,077,010,0198,91

1,9850,0152,000

0,4480,0530,0010,0010,502

0,4500,0530,0010,5050,0020,4870,0001,498

4,000

Bk 39828.8.92coes (i)

55,470,0412,130,003,073,370,006,0610,790,038,260,0199,23

1,9890,0112,000

0,5020,0830,0000,0010,585

0,3240,1010,0000,4150,0010,5740,0001,415

4,000

Bk 39928.8.92core

55,900,0411,780,022,242,880,016,9311,480,087,940,0199,31

1,9960,0042,000

0,4920,0600,0010,0010,553

0,3690,0860,0000,4390,0020,5500,0001,447

4,000

Bk 391028.8.92cpx

55,780,0310,940,023,792,060,007,2411,750,107,890,0199,61

1,9910,0092,000

0,4520,1020,0010,0010,555

0,3850,0610,0000,4490,0030,5460,0001,445

4,000

Bk 391128.8.92cpx

54,970,0510,670,036,392,470,006,0910,800,038,320,0099,82

1,9760,0242,000

0,4280,1730,0010,0010,603

0,3260,0740,0000,4160,0010,5800,0001,397

4,000

Bk 391328.8.92cpx

55,550,1711,080,022,993,020,037,0611,250,017,860,0199,05

1,9950,0052,000

0,4650,0810,0010,0030,549

0,3780,0910,0010,4330,0000,5470,0001,451

4,000

Bk 391428.8.92cpx

55,240,0711,130,002,473,010,007,2212,240,017,440,0198,84

1,9890,0112,000

0,4610,0670,0000,0010,530

0,3870,0910,0000,4720,0000,5190,0001,470

4,000

Bk 392928.8.92sympl

55,510,0611,390,022,162,680,027,7212,330,007,360,0199,26

1,9850,0152,000

0,4650,0580,0010,0010,525

0,4110,0800,0010,4720,0000,5100,0001,475

4,000



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 392228.1.93i (gnt)

55,270,0111,390,053,783,160,076,1110,530,268,230,0398,89

1,9940,0062,000

0,4790,1030,0010,0000,583

0,3290,0950,0020,4070,0070,5760,0011,417

4,000

Bk 392428.1.93i (gnt)

55,190,0110,950,124,482,640,036,7011,380,207,880,0399,61

1,9810,0192,000

0,4440,1210,0030,0000,569

0,3580,0790,0010,4380,0050,5480,0011,431

4,000

Bk 392528.1.93i (gnt)

54,990,2210,990,043,902,950,036,5911,280,207,840,0699,09

1,9840,0162,000

0,4520,1060,0010,0040,563

0,3540,0890,0010,4360,0050,5480,0031,437

4,000

Bk 392928.1.93i (gnt)

54,560,479,220,126,844,050,026,0411,020,187,850,01100,37

1,9750,0252,000

0,3680,1860,0030,0090,567

0,3260,1230,0010,4270,0050,5510,0001,433

4,000

Bk 393128.1.93i (gnt)

55,460,0711,000,025,632,490,056,039,730,088,730,0299,30

1,9940,0062,000

0,4600,1520,0010,0010,614

0,3230,0750,0020,3750,0020,6090,0011,386

4,000

Bk 393428.1.93i (gnt)

55,410,1110,990,066,012,400,565,8310,100,168,590,02100,23

1,9830,0172,000

0,4460,1620,0020,0020,612

0,3110,0720,0170,3870,0040,5960,0011,388

4,000

Bk 395528.1.93gnt

54,660,0510,540,075,111,660,357,2211,590,147,650,0299,06

1,9730,0272,000

0,4210,1390,0020,0010,563

0,3880,0500,0110,4480,0040,5350,0011,437

4,000

Bk 395728.1.93gnt

56,550,0311,210,002,442,930,037,5212,300,127,630,01100,77

1,9950,0052,000

0,4610,0650,0000,0010,527

0,3950,0860,0010,4650,0030,5220,0001,473

4,000

Bk 396028.1.93gnt

55,590,0610,820,023,091,910,028,0912,540,367,210,1199,82

1,9820,0182,000

0,4360,0830,0010,0010,521

0,4300,0570,0010,4790,0090,4980,0051,479

4,000

Bk 397228.1.93i (gnt)

54,860,0010,020,005,643,580,055,7810,580,298,150,0298,98

1,9960,0042,000

0,4260,1540,0000,0000,580

0,3130,1090,0020,4120,0080,5750,0011,420

4,000

Bk 39328.8.92coes (i)

55,560,0311,190,050,862,770,048,2112,790,007,030,0198,54

1,9950,0052,000

0,4690,0230,0010,0010,494

0,4390,0830,0010,4920,0000,4890,0001,506

4,000

Bk 393028.8.92cpx

55,850,0210,830,001,792,040,048,5913,480,006,930,0099,57

1,9880,0122,000

0,4420,0480,0000,0000,490

0,4560,0610,0010,5140,0000,4780,0001,510

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 393128.8.92cpx

55,550,0310,990,052,151,550,018,4813,090,077,090,0299,07

1,9850,0152,000

0,4470,0580,0010,0010,507

0,4520,0460,0000,5010,0020,4910,0011,493

4,000

Bk 393228.8.92cpx

55,560,0410,980,002,341,860,008,4013,100,007,070,0299,37

1,9820,0182,000

0,4440,0630,0000,0010,507

0,4470,0560,0000,5010,0000,4890,0011,493

4,000

Bk 393328.8.92cpx

55,420,049,790,012,681,430,049,4514,460,036,340,0199,70

1,9770,0232,000

0,3880,0720,0000,0010,461

0,5020,0430,0010,5530,0010,4380,0001,539

4,000

Bk 393428.8.92cpx

55,660,0911,060,002,571,260,018,4513,150,007,190,0399,48

1,9810,0192,000

0,4440,0690,0000,0020,515

0,4480,0380,0000,5010,0000,4960,0011,485

4,000

Bk 393528.8.92cpx

55,690,0610,970,001,891,750,008,6213,410,006,960,0299,37

1,9840,0162,000

0,4450,0510,0000,0010,496

0,4580,0520,0000,5120,0000,4810,0011,504

4,000

Bk 393628.8.92cpx

55,800,0610,580,032,321,610,028,6713,620,006,950,0099,66

1,9850,0152,000

0,4290,0620,0010,0010,493

0,4600,0480,0010,5190,0000,4790,0001,507

4,000

Bk 393728.8.92cpx

55,130,019,750,053,632,150,058,3213,270,136,840,0299,35

1,9820,0182,000

0,3950,0980,0010,0000,495

0,4460,0650,0020,5110,0030,4770,0011,505

4,000

Bk 393828.8.92core

55,470,0511,260,002,542,730,027,2411,990,057,600,0298,96

1,9920,0082,000

0,4680,0680,0000,0010,537

0,3870,0820,0010,4610,0010,5290,0011,463

4,000

Bk 393928.8.92cpx

55,330,049,540,002,712,890,008,4213,820,016,580,0299,36

1,9900,0102,000

0,3950,0730,0000,0010,469

0,4510,0870,0000,5330,0000,4590,0011,531

4,000

Bk 394028.8.92cpx

55,680,0111,070,021,602,120,058,3013,090,017,070,0299,04

1,9900,0102,000

0,4570,0430,0010,0000,500

0,4420,0630,0020,5010,0000,4900,0011,500

4,000

Bk 394128.8.92cpx

55,720,0611,450,021,542,140,068,2112,630,007,250,0199,09

1,9880,0122,000

0,4700,0410,0010,0010,513

0,4370,0640,0020,4830,0000,5020,0001,487

4,000

Bk 394228.8.92cpx

55,810,0511,230,031,562,250,038,3412,920,107,100,0299,44

1,9880,0122,000

0,4590,0420,0010,0010,503

0,4430,0670,0010,4930,0030,4900,0011,497

4,000

Bk 395328.8.92gnt

55,120,049,590,014,662,890,067,5812,950,157,030,05100,13

1,9790,0212,000

0,3850,1260,0000,0010,512

0,4060,0870,0020,4980,0040,4890,0021,488

4,000

Bk 395428.8.92gnt

54,360,039,670,004,322,910,107,3513,170,006,890,0398,82

1,9770,0232,000

0,3910,1180,0000,0010,510

0,3980,0880,0030,5130,0000,4860,0011,490

4,000

Bk 391,34.5.92gnt

56,000,0511,420,021,232,780,008,1112,41n.a.7,290,0299,32

1,9950,0052,000

0,4740,0330,0010,0010,509

0,4310,0830,0000,474-0,5030,0011,491

4,000

Bk 392,24.5.92i (gnt)

55,420,0411,450,023,352,940,016,5911,02n.a.8,070,0298,93

1,9930,0072,000

0,4780,0910,0010,0010,570

0,3530,0880,0000,425-0,5630,0011,430

4,000

Bk 392,34.5.92gnt

56,090,0111,540,041,462,550,027,7812,36n.a.7,500,0199,36

1,9970,0032,000

0,4810,0390,0010,0000,521

0,4130,0760,0010,471-0,5180,0001,479

4,000

Bk 396,24.5.92i (gnt)

55,090,0210,480,093,803,080,046,7911,86n.a.7,650,0098,90

1,9910,0092,000

0,4380,1030,0030,0000,544

0,3660,0930,0010,459-0,5360,0001,456

4,000

Bk 397,24.5.92i (gnt)

55,170,0211,030,053,853,290,056,4811,24n.a.7,900,0299,10

1,9890,0112,000

0,4580,1040,0010,0000,564

0,3480,0990,0020,434-0,5520,0011,436

4,000

Bk 398,24.5.92i (gnt)

55,200,0412,010,003,402,240,056,4310,78n.a.8,290,0198,45

1,9880,0122,000

0,4980,0920,0000,0010,591

0,3450,0670,0020,416-0,5790,0001,409

4,000

Bk 399,24.5.92gnt

55,830,0610,610,011,072,680,048,5513,38n.a.6,830,0199,07

1,9980,0022,000

0,4450,0290,0000,0010,475

0,4560,0800,0010,513-0,4740,0001,525

4,000

Bk 3910,24.5.92gnt

55,640,0410,630,010,882,920,018,4113,06n.a.6,880,0098,49

2,0020,0002,002

0,4520,0240,0000,0010,477

0,4510,0880,0000,503-0,4800,0001,523

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 3913,24.5.92gnt

55,750,0311,310,012,451,920,037,9012,37n.a.7,500,0199,28

1,9880,0122,000

0,4640,0660,0000,0010,530

0,4200,0570,0010,473-0,5190,0001,470

4,000

Bk 3914,24.5.92gnt

55,470,0310,290,052,422,290,038,2613,05n.a.7,020,0198,92

1,9930,0072,000

0,4290,0650,0010,0010,496

0,4420,0690,0010,502-0,4890,0001,504

4,000

Bk 392,15.5.92par

55,320,0510,740,002,102,450,057,9212,68n.a.7,180,0198,50

1,9930,0072,000

0,4500,0570,0000,0010,508

0,4250,0740,0020,490-0,5020,0001,492

4,000

Bk 393,15.5.92core

55,490,0712,600,002,803,510,045,509,76n.a.8,730,0298,52

1,9990,0012,000

0,5330,0760,0000,0010,611

0,2950,1060,0010,377-0,6100,0011,389

4,000

Bk 393,25.5.92clz

55,450,0510,900,052,722,780,017,2611,78n.a.7,660,0098,65

1,9980,0022,000

0,4600,0740,0010,0010,536

0,3900,0840,0000,455-0,5350,0001,464

4,000

Bk 394,15.5.92core

55,720,0412,560,012,563,670,015,639,69n.a.8,720,0398,64

2,0030,0002,003

0,5350,0690,0000,0010,605

0,3020,1100,0000,373-0,6080,0011,395

4,000

Bk 394,25.5.92clz

55,520,0710,870,042,103,090,007,2012,22n.a.7,510,0198,63

2,0010,0002,001

0,4630,0570,0010,0010,523

0,3870,0930,0000,472-0,5250,0001,477

4,000

Bk 395,15.5.92cpx

55,340,0411,090,042,522,390,017,3111,92n.a.7,650,0198,31

1,9970,0032,000

0,4680,0680,0010,0010,538

0,3930,0720,0000,461-0,5350,0001,462

4,000

Bk 396,15.5.92cpx

55,500,0311,430,002,452,600,007,1811,69n.a.7,760,0198,65

1,9950,0052,000

0,4790,0660,0000,0010,546

0,3850,0780,0000,450-0,5410,0001,454

4,000

Bk 397,15.5.92core

55,540,0612,230,002,142,850,006,3310,63n.a.8,340,0198,12

2,0020,0002,002

0,5210,0580,0000,0010,580

0,3400,0860,0000,410-0,5830,0001,420

4,000Bk

398,15.5.92cpx

55,570,0712,460,042,873,090,005,709,71n.a.8,780,0398,32

2,0020,0002,002

0,5310,0780,0010,0010,611

0,3060,0930,0000,375-0,6130,0011,389

4,000

Bk 399,15.5.92core

55,510,0611,140,031,302,410,028,0512,73n.a.7,180,0198,44

1,9950,0052,000

0,4670,0350,0010,0010,504

0,4310,0730,0010,490-0,5000,0001,496

4,000

Bk 3910,15.5.92par

54,970,0411,300,012,563,210,017,5411,09n.a.7,510,0298,27

1,9870,0132,000

0,4690,0700,0000,0010,539

0,4060,0970,0000,430-0,5260,0011,461

4,000

Bk 3911,15.5.92par

55,330,0311,130,033,462,300,047,0211,48n.a.7,890,0198,73

1,9920,0082,000

0,4640,0940,0010,0010,559

0,3770,0690,0010,443-0,5510,0001,441

4,000

Bk 73825.6.92gnt

54,910,0310,040,042,562,820,087,9013,62n.a.6,740,0098,74

1,9860,0142,000

0,4140,0700,0010,0010,486

0,4260,0850,0020,528-0,4730,0001,514

4,000

Bk 7226.4.93gnt

56,240,0311,670,031,832,720,087,4711,560,297,770,0299,70

1,9980,0022,000

0,4870,0490,0010,0010,537

0,3960,0810,0020,4400,0080,5350,0011,463

4,000

Bk 7326.4.93gnt

56,070,1512,230,130,733,720,077,0911,260,227,770,0299,46

1,9980,0022,000

0,5110,0200,0040,0030,537

0,3760,1110,0020,4300,0060,5370,0011,463

4,000

Bk 73826.4.93i (gnt)

55,970,1110,270,001,403,860,067,7112,390,097,200,0099,06

2,0120,0002,012

0,4350,0380,0000,0020,475

0,4130,1160,0020,4770,0020,5020,0001,512

4,000

Bk 74026.4.93i (gnt)

56,310,0412,120,102,422,420,026,9910,720,158,310,0299,62

1,9980,0022,000

0,5050,0650,0030,0010,574

0,3700,0720,0010,4080,0040,5720,0011,426

4,000

Bk 74126.4.93i (gnt)

55,340,0410,910,032,003,870,097,4611,530,127,320,0498,75

1,9970,0032,000

0,4610,0540,0010,0010,517

0,4010,1170,0030,4460,0030,5120,0021,483

4,000

Bk 74226.4.93i (gnt)

55,100,0710,890,032,224,010,097,1211,960,217,240,0298,96

1,9900,0102,000

0,4540,0600,0010,0010,516

0,3830,1210,0030,4630,0060,5070,0011,484

4,000

Bk 71527.8.92par

54,970,0410,570,073,332,010,077,7013,190,137,090,0299,19

1,9770,0232,000

0,4250,0900,0020,0010,518

0,4130,0600,0020,5080,0030,4940,0011,482

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 71627.8.92core

55,870,0613,120,081,482,840,006,7710,410,278,260,0299,18

1,9880,0122,000

0,5390,0400,0020,0010,581

0,3590,0850,0000,3970,0070,5700,0011,419

4,000

Bk 71727.8.92par

55,180,0510,690,063,092,210,037,6613,260,267,090,0199,59

1,9770,0232,000

0,4290,0830,0020,0010,515

0,4090,0660,0010,5090,0070,4930,0001,485

4,000

Bk 71827.8.92par

55,030,0410,510,001,253,920,067,5313,330,396,680,0198,74

1,9930,0072,000

0,4410,0340,0000,0010,476

0,4060,1190,0020,5170,0100,4690,0001,524

4,000

Bk 72827.8.92gl

55,520,0210,900,031,003,130,068,1213,610,136,720,0199,25

1,9890,0112,000

0,4490,0270,0010,0000,478

0,4340,0940,0020,5220,0030,4670,0001,522

4,000

Bk 73027.8.92cpx

54,740,029,520,092,651,840,068,8614,760,346,160,0099,05

1,9750,0252,000

0,3800,0720,0030,0000,455

0,4770,0560,0020,5710,0090,4310,0001,545

4,000

Bk 73527.8.92par

54,930,0510,960,052,042,400,037,9513,220,106,900,0398,66

1,9800,0202,000

0,4450,0550,0010,0010,503

0,4270,0720,0010,5100,0030,4820,0011,497

4,000

Bk 73727.8.92par

54,610,019,570,032,832,150,028,5014,720,256,220,0298,93

1,9750,0252,000

0,3830,0770,0010,0000,462

0,4580,0650,0010,5710,0070,4360,0011,538

4,000

Bk 73827.8.92core

55,350,0511,110,031,163,040,058,0313,290,276,790,0299,20

1,9850,0152,000

0,4540,0310,0010,0010,487

0,4290,0910,0020,5110,0070,4720,0011,513

4,000

Bk 73927.8.92core

54,800,0510,990,032,311,880,058,0513,590,306,810,0198,87

1,9720,0282,000

0,4380,0630,0010,0010,503

0,4320,0570,0020,5240,0080,4750,0001,497

4,000

Bk 74027.8.92core

54,330,019,760,012,522,010,058,7314,710,156,100,0398,40

1,9720,0282,000

0,3890,0690,0000,0000,459

0,4720,0610,0020,5720,0040,4290,0011,541

4,000

Bk 74127.8.92par

54,670,029,470,013,960,840,069,0814,770,246,270,0399,42

1,9650,0352,000

0,3660,1070,0000,0000,473

0,4860,0250,0020,5690,0060,4370,0011,527

4,000

Bk 7446.7.92i (gnt)

55,340,049,820,062,693,800,067,6212,99n.a.6,920,0199,35

1,9950,0052,000

0,4130,0730,0020,0010,488

0,4100,1140,0020,502-0,4840,0001,512

4,000

Bk 74227.8.92cpx

54,510,039,900,001,852,580,068,5414,390,176,180,0398,25

1,9810,0192,000

0,4040,0510,0000,0010,456

0,4620,0780,0020,5600,0050,4350,0011,544

4,000

Bk 75127.8.92gl

55,320,0111,130,002,792,190,057,5912,860,267,250,0299,47

1,9800,0202,000

0,4490,0750,0000,0000,524

0,4050,0660,0020,4930,0070,5030,0011,476

4,000

Bk 75327.8.92clz

54,910,0510,430,002,303,030,047,6413,500,226,790,0198,92

1,9840,0162,000

0,4280,0630,0000,0010,491

0,4110,0920,0010,5230,0060,4760,0001,509

4,000

Bk 776.7.92core

55,380,0511,700,022,202,160,007,3111,95n.a.7,710,0098,48

1,9900,0102,000

0,4850,0590,0010,0010,546

0,3920,0650,0000,460-0,5370,0001,454

4,000

Bk 786.7.92core

55,080,0310,730,031,453,740,057,3613,08n.a.6,940,0198,51

1,9940,0062,000

0,4520,0400,0010,0010,493

0,3970,1130,0020,507-0,4870,0001,507

4,000

Bk 7126.7.92gnt

55,650,0611,060,022,832,920,027,0511,93n.a.7,720,0099,25

1,9950,0052,000

0,4620,0760,0010,0010,540

0,3770,0870,0010,458-0,5370,0001,460

4,000

Bk 7136.7.92i (gnt)

55,810,0612,850,021,562,330,026,7410,77n.a.8,320,0198,50

1,9950,0052,000

0,5370,0420,0010,0010,581

0,3590,0700,0010,413-0,5770,0001,419

4,000

Bk 7146.7.92i (gnt)

55,230,0512,350,033,021,860,006,7310,94n.a.8,240,0098,44

1,9830,0172,000

0,5060,0820,0010,0010,589

0,3600,0560,0000,421-0,5740,0001,411

4,000

Bk 7186.7.92amph

54,040,018,180,003,673,350,088,1814,97n.a.5,910,0198,40

1,9830,0172,000

0,3370,1010,0000,0000,438

0,4470,1030,0020,588-0,4200,0001,562

4,000

Bk 7236.7.92gnt

55,600,0311,830,002,292,300,047,1111,55n.a.7,900,0298,67

1,9940,0062,000

0,4940,0620,0000,0010,556

0,3800,0690,0010,444-0,5490,0011,444

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 7456.7.92i (gnt)

54,990,029,990,102,873,290,137,6813,22n.a.6,840,0099,14

1,9860,0142,000

0,4110,0780,0030,0000,493

0,4130,1000,0040,512-0,4790,0001,507

4,000

Bk 7476.7.92i (gnt)

55,510,0211,860,022,652,180,046,9711,30n.a.8,030,0198,60

1,9920,0082,000

0,4940,0720,0010,0000,567

0,3730,0660,0010,435-0,5590,0001,433

4,000

Bk 7556.7.92gnt

54,750,0310,080,083,973,140,127,1612,09n.a.7,320,0198,75

1,9860,0142,000

0,4170,1080,0020,0010,528

0,3870,0950,0040,470-0,5150,0001,472

4,000

Bk 7646.7.92i (gnt)

55,100,0410,380,082,992,910,027,2512,16n.a.7,430,0198,37

1,9970,0032,000

0,4400,0820,0020,0010,525

0,3920,0880,0010,472-0,5220,0001,475

4,000

Bk 7686.7.92gnt

55,030,0310,430,043,752,760,007,4312,83n.a.7,200,0099,50

1,9780,0222,000

0,4200,1010,0010,0010,523

0,3980,0830,0000,494-0,5020,0001,477

4,000

Bk 7746.7.92sympl

55,140,0210,580,031,883,210,037,5612,55n.a.7,150,0098,15

1,9990,0012,000

0,4510,0510,0010,0000,503

0,4080,0970,0010,487-0,5030,0001,497

4,000

Bk 737.7.92amph

55,390,0610,820,011,763,400,007,4212,92n.a.7,130,0198,93

1,9940,0062,000

0,4530,0480,0000,0010,503

0,3980,1020,0000,498-0,4980,0001,497

4,000

Bk 747.7.92calcit

54,820,0110,450,002,282,780,077,6213,43n.a.6,870,0298,35

1,9870,0132,000

0,4340,0620,0000,0000,496

0,4120,0840,0020,522-0,4830,0011,504

4,000

Bk 767.7.92amph

54,850,0210,570,012,962,380,057,6413,14n.a.7,050,0198,68

1,9810,0192,000

0,4310,0800,0000,0000,512

0,4110,0720,0020,509-0,4940,0001,488

4,000

Bk 7217.7.92i (gnt)

55,190,0611,300,073,481,780,087,3312,07n.a.7,680,0199,05

1,9790,0212,000

0,4570,0940,0020,0010,554

0,3920,0530,0020,464-0,5340,0001,446

4,000

Bk 7247.7.92i (gnt)

55,310,0212,030,002,262,760,006,9711,24n.a.7,880,0198,48

1,9890,0112,000

0,4990,0610,0000,0000,560

0,3740,0830,0000,433-0,5490,0001,440

4,000

Bk 7287.7.92i (gnt)

55,140,0711,390,073,731,460,017,1811,88n.a.7,870,0098,80

1,9800,0202,000

0,4620,1010,0020,0010,566

0,3840,0440,0000,457-0,5480,0001,434

4,000

Bk 7297.7.92i (gnt)

54,710,0410,340,064,112,940,066,7812,39n.a.7,430,0198,87

1,9830,0172,000

0,4240,1120,0020,0010,539

0,3660,0890,0020,481-0,5220,0001,461

4,000

Bk 7327.7.92i (gnt)

54,450,0810,050,013,773,120,087,1512,50n.a.7,160,0098,37

1,9840,0162,000

0,4150,1030,0000,0020,520

0,3880,0950,0020,488-0,5060,0001,480

4,000

Bk 7427.7.92par

55,810,0512,410,022,092,490,026,7010,99n.a.8,240,0198,83

1,9950,0052,000

0,5180,0560,0010,0010,576

0,3570,0740,0010,421-0,5710,0001,424

4,000

Bk 7457.7.92gnt

55,100,0410,670,003,402,160,007,4013,13n.a.7,270,0199,18

1,9810,0192,000

0,4330,0920,0000,0010,526

0,3970,0650,0000,506-0,5070,0001,474

4,000

Bk 7467.7.92gnt

54,950,0711,380,052,453,750,097,2911,76n.a.7,280,0399,11

1,9780,0222,000

0,4610,0660,0010,0010,530

0,3910,1130,0030,454-0,5080,0011,470

4,000

Bk 7507.7.92gnt

54,720,0410,700,003,351,960,097,4513,15n.a.7,170,0198,65

1,9770,0232,000

0,4330,0910,0000,0010,525

0,4010,0590,0030,509-0,5020,0001,475

4,000

Bk 81414.3.93cpx

56,340,0313,310,052,461,470,036,8210,500,218,260,57100,09

1,9850,0152,000

0,5380,0650,0010,0010,605

0,3580,0430,0010,3960,0050,5640,0261,395

4,000

Bk 83614.3.93gnt

55,360,0611,210,002,272,360,057,5013,030,157,240,0299,25

1,9840,0162,000

0,4570,0610,0000,0010,519

0,4010,0710,0020,5000,0040,5030,0011,481

4,000

Bk 83714.3.93gnt

55,560,0311,520,002,252,430,017,5012,580,237,390,0299,51

1,9830,0172,000

0,4680,0600,0000,0010,529

0,3990,0730,0000,4810,0060,5110,0011,471

4,000

Bk 83814.3.93gnt

55,250,1010,510,001,013,540,058,0913,520,136,610,0198,82

1,9920,0082,000

0,4390,0270,0000,0020,468

0,4350,1070,0020,5220,0030,4620,0001,532

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Bk 83914.3.93gnt

55,830,0110,960,000,903,410,077,9413,290,216,870,0299,51

1,9950,0052,000

0,4570,0240,0000,0000,481

0,4230,1020,0020,5090,0060,4760,0011,519

4,000

Bk 84014.3.93core

56,070,0412,370,032,662,360,006,5710,690,218,410,0499,45

1,9950,0052,000

0,5140,0710,0010,0010,586

0,3480,0700,0000,4080,0060,5800,0021,414

4,000

Bk 84114.3.93core

55,970,0510,990,001,833,030,017,6813,070,157,140,0899,99

1,9920,0082,000

0,4530,0490,0000,0010,503

0,4070,0900,0000,4980,0040,4930,0041,497

4,000

Bk 84214.3.93cpx

55,560,0110,550,042,432,950,057,5713,010,167,130,0299,51

1,9920,0082,000

0,4380,0660,0010,0000,504

0,4050,0890,0020,5000,0040,4960,0011,496

4,000

Bk 84314.3.93cpx

55,700,0510,860,011,823,680,077,1412,930,267,180,0299,74

1,9950,0052,000

0,4530,0490,0000,0010,504

0,3810,1100,0020,4960,0070,4990,0011,496

4,000

Bk 84414.3.93core

56,310,0212,190,021,162,570,077,4611,310,327,880,0399,35

2,0010,0002,001

0,5100,0310,0010,0000,542

0,3950,0770,0020,4310,0080,5430,0011,457

4,000

Bk 8329.1.93arut

55,960,4112,460,030,612,770,007,6011,260,427,670,1699,35

1,9910,0092,000

0,5130,0160,0010,0080,538

0,4030,0820,0000,4290,0110,5290,0071,462

4,000

Bk 8429.1.93arut

55,550,3012,070,030,163,640,057,3911,290,147,570,0298,22

2,0000,0002,000

0,5120,0040,0010,0060,523

0,3970,1100,0020,4360,0040,5280,0011,477

4,000

Bk 8529.1.93aap

55,120,1911,470,020,504,140,237,1212,060,127,200,0198,18

1,9970,0032,000

0,4870,0140,0010,0040,505

0,3850,1250,0070,4680,0030,5060,0001,495

4,000

Bk 8629.1.93acore

55,660,1112,400,090,933,200,356,9811,340,177,740,0298,99

1,9920,0082,000

0,5140,0250,0030,0020,544

0,3720,0960,0110,4350,0040,5370,0011,456

4,000

Bk 81429.1.93agnt

55,370,0411,190,022,352,430,077,7412,910,177,150,0399,48

1,9800,0202,000

0,4520,0630,0010,0010,516

0,4130,0730,0020,4950,0040,4960,0011,484

4,000

Bk 82029.1.93agnt

55,980,0513,640,042,231,830,026,459,900,198,780,0299,13

1,9860,0142,000

0,5560,0600,0010,0010,618

0,3410,0540,0010,3760,0050,6040,0011,382

4,000

Bk 82129.1.93agnt

55,320,0211,380,032,912,670,047,1011,210,077,830,0298,60

1,9920,0082,000

0,4750,0790,0010,0000,555

0,3810,0810,0010,4330,0020,5470,0011,445

4,000

Bk 82329.1.93agnt

55,480,0211,560,001,962,640,037,6012,530,187,290,0499,33

1,9830,0172,000

0,4700,0530,0000,0000,523

0,4050,0790,0010,4800,0050,5050,0021,477

4,000

Bk 82629.1.93ai (rut)

55,660,2713,240,000,143,320,036,8310,120,198,190,0398,02

1,9990,0012,000

0,5590,0040,0000,0050,568

0,3660,1000,0010,3890,0050,5700,0011,432

4,000

Bk 8129.1.93bi (rut)

56,240,2613,880,002,191,350,056,609,910,208,910,0299,61

1,9830,0172,000

0,5590,0580,0000,0050,622

0,3470,0400,0010,3740,0050,6090,0011,378

4,000

Bk 81129.1.93bcore

56,270,1612,540,012,211,660,017,2810,990,118,310,0199,56

1,9910,0092,000

0,5140,0590,0000,0030,576

0,3840,0490,0000,4170,0030,5700,0001,424

4,000

Bk 81229.1.93bsympl

56,230,0813,650,060,672,950,036,4910,320,288,450,0399,24

1,9950,0052,000

0,5650,0180,0020,0020,586

0,3430,0870,0010,3920,0070,5810,0011,414

4,000

Bk 83629.1.93bcore

55,980,0012,200,000,942,870,027,3510,870,207,940,0198,37

2,0060,0002,006

0,5210,0250,0000,0000,546

0,3930,0860,0010,4170,0050,5520,0001,454

4,000

Bk 83729.1.93bcore

55,840,0412,140,040,333,390,047,4811,370,007,650,0098,31

2,0040,0002,004

0,5170,0090,0010,0010,528

0,4000,1020,0010,4370,0000,5320,0001,472

4,000

Bk 83829.1.93bcore

56,020,0312,220,032,951,090,017,5411,270,547,970,1999,87

1,9830,0172,000

0,4920,0790,0010,0010,572

0,3980,0320,0000,4270,0140,5470,0091,428

4,000

Bk 83929.1.93bcore

56,210,0312,250,050,004,150,037,1610,950,217,760,0398,35

2,0170,0002,017

0,5350,0000,0010,0010,524

0,3830,1250,0010,4210,0060,5400,0011,476

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Cig 90/40456.1.91cpx

55,680,0411,830,001,783,410,046,8610,84n.a.7,980,0198,49

2,0030,0002,003

0,5020,0480,0000,0010,550

0,3680,1030,0010,418-0,5570,0001,447

4,000

Cig 90/40536.1.91i (gnt)

53,180,0310,680,024,325,360,086,8412,16n.a.6,550,0199,22

1,9420,0582,000

0,4020,1190,0010,0010,522

0,3720,1640,0020,476-0,4640,0001,478

4,000

Cig 90/40556.1.91i (gnt)

55,380,0611,220,002,323,890,107,2412,28n.a.7,240,0299,75

1,9830,0172,000

0,4560,0630,0000,0010,520

0,3860,1160,0030,471-0,5030,0011,480

4,000

Cig 90/4036.1.91ai (gnt)

55,290,0411,390,032,473,100,046,8911,31n.a.7,800,0098,50

1,9960,0042,000

0,4800,0670,0010,0010,549

0,3710,0930,0010,437-0,5460,0001,451

4,000

Cig 90/4046.1.91ai (gnt)

54,690,059,430,032,435,070,017,0512,79n.a.6,760,0098,41

2,0020,0002,002

0,4070,0670,0010,0010,476

0,3850,1550,0000,502-0,4800,0001,523

4,000

Cig 90/4026.1.91bi (gnt)

54,870,039,280,041,896,000,026,8612,86n.a.6,660,0198,52

2,0090,0002,009

0,4000,0520,0010,0010,454

0,3740,1840,0010,505-0,4730,0001,536

4,000

Cig 90/4036.1.91bi (gnt)

54,370,048,930,054,584,340,066,5912,26n.a.7,150,0198,38

1,9970,0032,000

0,3830,1270,0010,0010,512

0,3610,1330,0020,482-0,5090,0001,488

4,000

Cig 90/4066.1.91bi (gnt)

54,820,059,750,052,624,940,006,9812,80n.a.6,860,0098,86

1,9950,0052,000

0,4140,0720,0010,0010,488

0,3790,1500,0000,499-0,4840,0001,512

4,000

Cig 90/4076.1.91bi (gnt)

54,770,058,450,073,015,460,027,5113,74n.a.6,260,0099,40

1,9960,0042,000

0,3590,0830,0020,0010,445

0,4080,1660,0010,537-0,4420,0001,555

4,000

Cig 90/40436.1.91bcoes (i)

55,140,0510,640,011,903,950,007,3711,73n.a.7,300,0098,09

2,0020,0002,002

0,4550,0520,0000,0010,508

0,3990,1200,0000,456-0,5140,0001,489

4,000

Cig 90/40446.1.91bcoes (i)

55,740,0311,490,002,402,960,047,1311,33n.a.7,860,0098,98

1,9970,0032,000

0,4830,0650,0000,0010,548

0,3810,0890,0010,435-0,5460,0001,452

4,000

Cig 90/4031?coes (i)

55,800,0411,000,002,623,040,007,3011,70n.a.7,700,0099,20

1,9990,0012,000

0,4640,0710,0000,0010,535

0,3900,0910,0000,449-0,5350,0001,465

4,000


55,600,0511,300,003,262,370,007,1011,60n.a.7,900,0099,18

1,9910,0092,000

0,4680,0880,0000,0010,557

0,3790,0710,0000,445-0,5480,0001,443

4,000

Cig 90/4033?par

56,000,0412,100,002,242,880,006,8010,90n.a.8,200,0099,16

1,9980,0022,000

0,5070,0600,0000,0010,568

0,3620,0860,0000,417-0,5670,0001,432

4,000

Cig 90/4043?par (i)

55,200,0510,300,001,933,260,007,9013,40n.a.6,800,0098,84

1,9920,0082,000

0,4300,0530,0000,0010,483

0,4250,0980,0000,518-0,4760,0001,517

4,000

Cig 90/4044?par (i)

55,800,0410,700,001,673,500,007,6013,10n.a.7,100,0099,51

1,9970,0032,000

0,4490,0450,0000,0010,495

0,4050,1050,0000,502-0,4930,0001,505

4,000


55,500,0511,700,003,531,630,007,1011,00n.a.8,200,0098,70

1,9890,0112,000

0,4840,0950,0000,0010,580

0,3790,0490,0000,422-0,5700,0001,420

4,000


55,700,0511,500,003,132,280,007,1011,40n.a.8,000,0099,16

1,9920,0082,000

0,4770,0840,0000,0010,562

0,3780,0680,0000,437-0,5550,0001,438

4,000

Cig 90/4048?i (gnt)

55,900,0512,100,001,613,050,006,9010,90n.a.8,100,0098,61

2,0030,0002,003

0,5110,0430,0000,0010,555

0,3690,0920,0000,419-0,5630,0001,441

4,000

Cig 90/4063?i (gnt)

55,600,0411,900,003,392,350,076,6010,80n.a.8,300,0099,05

1,9910,0092,000

0,4930,0910,0000,0010,585

0,3520,0700,0020,414-0,5760,0001,415

4,000

Cig 90/4064?i (gnt)

55,500,0512,000,003,361,680,007,0011,10n.a.8,200,0098,89

1,9850,0152,000

0,4910,0900,0000,0010,583

0,3730,0500,0000,425-0,5690,0001,417

4,000

Cig 90/4065?cpx

54,900,0510,200,003,044,470,006,7012,40n.a.7,200,0098,95

1,9930,0072,000

0,4290,0830,0000,0010,513

0,3620,1360,0000,482-0,5070,0001,487

4,000







SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum



SiAlt

AloFe3CrTi

MgFe2MnCaZnNaK

sum

Cig 90/4066?cpx

55,700,0611,700,004,161,360,007,1011,40n.a.8,200,0099,68

1,9810,0192,000

0,4710,1110,0000,0010,583

0,3760,0400,0000,434-0,5650,0001,417

4,000

Cig 90/4067?cpx

55,400,0511,400,002,792,690,007,0011,30n.a.7,900,0098,53

1,9950,0052,000

0,4790,0760,0000,0010,556

0,3760,0810,0000,436-0,5520,0001,444

4,000

Cig 90/4068?cpx

55,300,0010,900,002,772,910,007,1011,60n.a.7,700,0098,28

2,0000,0002,000

0,4650,0750,0000,0000,540

0,3830,0880,0000,449-0,5400,0001,460

4,000

Cig 91-1516.6.93cpx

56,340,0310,680,021,423,440,048,0712,940,157,070,01100,21

2,0000,0002,000

0,4470,0380,0010,0010,486

0,4270,1020,0010,4920,0040,4870,0001,514

4,000

Cig 91-1716.6.93gnt

56,690,0411,710,001,983,040,007,1611,330,078,040,05100,11

2,0060,0002,006

0,4880,0530,0000,0010,542

0,3780,0900,0000,4290,0020,5520,0021,453

4,000

Cig 91-13316.6.93coes (i)

56,850,0411,520,011,742,860,017,6712,200,047,700,03100,67

2,0010,0002,001

0,4780,0460,0000,0010,525

0,4020,0840,0000,4600,0010,5250,0011,475

4,000

Cig 91-13416.6.93coes (i)

56,570,0311,570,001,264,020,047,1111,880,017,680,03100,20

2,0060,0002,006

0,4830,0340,0000,0010,518

0,3760,1190,0010,4510,0000,5280,0011,477

4,000

Cig 91-13516.6.93cpx

56,330,0010,630,021,653,770,057,5812,770,047,240,02100,10

2,0050,0002,005

0,4460,0440,0010,0000,491

0,4020,1120,0020,4870,0010,5000,0011,504

4,000

Cig 91-1628.11.93phe

56,010,0411,020,012,152,900,077,1811,750,017,780,0398,96

2,0080,0002,008

0,4660,0580,0000,0010,525

0,3840,0870,0020,4510,0000,5410,0011,467

4,000

Cig 91-11128.11.93phe

56,080,0510,680,022,313,620,077,3812,700,097,290,03100,32

1,9960,0042,000

0,4440,0620,0010,0010,507

0,3920,1080,0020,4840,0020,5030,0011,493

4,000

Cig 91-11228.11.93phe

56,230,1010,680,071,574,340,067,2512,790,067,220,02100,39

2,0020,0002,002

0,4480,0420,0020,0020,494

0,3850,1290,0020,4880,0020,4980,0011,504

4,000

Cig 91-1316.6.93coes (i)

56,820,0411,860,001,473,260,037,1511,150,008,100,0399,91

2,0110,0002,011

0,4950,0390,0000,0010,535

0,3770,0960,0010,4230,0000,5560,0011,454

4,000

Cig 91-1416.6.93coes (i)

56,930,0111,240,010,584,290,007,4312,200,027,520,01100,24

2,0160,0002,016

0,4690,0150,0000,0000,485

0,3920,1270,0000,4630,0010,5160,0001,499

4,000

Cig 91-1816.6.93gnt

56,960,0412,030,011,972,720,047,0410,890,008,370,02100,10

2,0100,0002,010

0,5000,0520,0000,0010,554

0,3700,0800,0010,4120,0000,5730,0011,437

4,000

C-15Appendix C Table C4 garnet

normed to 24 oxygens, Fe3 over charge balance


position means analysis of: core is core position in a grt grain, mineral x, rim position in grt grain in contact withmineral x, mineral x(i), grt at an inclusion of mineral x in grt


SiO2TiO2Al2O3Cr2O3Fe2O3FeOMnOMgOCaOtotal

SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 10B3319.10.93achl

37,650,0621,100,220,6328,290,803,827,3099,87

5,9510,049

3,8810,0750,0270,0053,995

0,9003,7400,1071,2365,983

15,978



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 10B3419.10.93achl

37,340,0620,860,001,5627,970,334,227,2399,58

5,8970,103

3,7790,1860,0000,0053,985

0,9933,6940,0441,2235,955

15,940

Bk 10B3519.10.93achl

37,420,1220,710,001,3527,370,802,978,9499,69

5,9300,070

3,7980,1610,0000,0103,982

0,7023,6280,1071,5185,954

15,937

Bk 10B3619.10.93achl

37,790,1121,090,041,2128,140,943,138,45100,90

5,9230,077

3,8190,1430,0050,0093,987

0,7313,6880,1251,4195,963

15,951

Bk 10B119.10.93bcore

36,720,0220,520,002,1226,353,262,088,7699,83

5,8510,149

3,7050,2540,0000,0023,981

0,4943,5120,4401,4965,941

15,923


36,830,1220,570,031,9224,963,882,009,5499,85

5,8610,139

3,7190,2300,0040,0103,981

0,4743,3220,5231,6275,946

15,927


37,050,1120,450,001,5526,411,922,529,1199,11

5,9190,081

3,7700,1860,0000,0093,980

0,6003,5290,2601,5595,948

15,928

Bk 10B419.10.93bchl

37,350,1420,710,011,5125,990,803,499,3299,32

5,9120,088

3,7750,1800,0010,0123,982

0,8233,4410,1071,5815,952

15,933

Bk 10B127.11.93chl

37,500,0821,130,010,9927,280,644,217,6499,48

5,9230,077

3,8570,1170,0010,0073,991

0,9913,6040,0861,2935,973

15,965

Bk 10B3027.11.93chl

37,460,0620,990,061,1027,880,983,228,2199,96

5,9240,076

3,8360,1310,0080,0053,990

0,7593,6870,1311,3915,969

15,958

Bk 10B3127.11.93chl

37,640,0720,870,051,2728,040,892,958,59100,38

5,9320,068

3,8090,1510,0060,0063,985

0,6933,6960,1191,4515,959

15,943

Bk 10B3427.11.93chl

37,400,0820,910,001,0027,920,783,308,0899,47

5,9390,061

3,8530,1200,0000,0073,989

0,7813,7080,1051,3755,969

15,957

Bk 10B3527.11.93chl

37,780,0820,910,051,0327,850,853,537,99100,07

5,9550,045

3,8400,1230,0060,0073,985

0,8293,6710,1131,3495,963

15,949

Bk 10B3627.11.93core

37,570,1620,770,031,3025,832,312,689,48100,13

5,9330,067

3,7990,1540,0040,0143,982

0,6313,4120,3091,6045,956

15,937

Bk 10B3727.11.93chl

37,330,0620,990,001,4928,200,863,697,44100,06

5,8890,111

3,7910,1770,0000,0053,988

0,8683,7200,1151,2575,960

15,948

Bk 10B3827.11.93chl

37,780,0521,160,021,1427,780,684,047,67100,31

5,9260,074

3,8370,1340,0020,0043,989

0,9443,6430,0901,2895,967

15,956

Bk 10B4027.11.93chl

38,050,0221,430,010,7124,711,603,5310,23100,29

5,9510,049

3,9000,0840,0010,0023,993

0,8233,2320,2121,7145,981

15,973

BK 17493.7.94chl

37,670,0521,020,000,2729,120,333,357,4099,21

6,0050,000

3,9490,0330,0000,0043,991

0,7963,8810,0451,2645,986

15,981

Bk 1825.8.94chl

38,020,0721,410,010,8927,161,053,978,18100,76

5,9340,066

3,8730,1040,0010,0063,992

0,9243,5460,1391,3685,976

15,968

Bk 1835.8.94chl

37,580,1521,310,020,9927,111,423,029,01100,61

5,9060,094

3,8530,1170,0020,0133,993

0,7073,5630,1891,5175,977

15,970

Bk 1855.8.94core

37,750,1421,170,000,7921,425,072,4211,31100,07

5,9470,053

3,8770,0940,0000,0123,989

0,5682,8210,6761,9095,975

15,964

Bk 1865.8.94chl

37,800,0521,230,000,7826,193,153,837,18100,21

5,9500,050

3,8880,0920,0000,0043,991

0,8993,4480,4201,2115,977

15,968

C-16 Appendix C Table C4 garnet




Bk 1885.8.94chl

37,690,0921,320,040,7327,231,522,948,92100,48

5,9330,067

3,8890,0870,0050,0083,995

0,6903,5850,2031,5055,982

15,977

Bk 1896.8.94core

38,110,0920,980,060,0023,952,622,5910,8099,20

6,0550,000

3,9290,0000,0080,0083,969

0,6133,1830,3531,8385,987

16,011



SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 397,213.3.93amph (i)

36,642,7520,780,120,0528,400,763,327,68100,51

5,8320,168

3,7310,0060,0150,2353,988

0,7883,7810,1021,3105,981

15,968

Bk 3911,213.3.93core

37,100,1020,750,001,5825,981,662,769,5899,51

5,8900,110

3,7720,1890,0000,0093,984

0,6533,4490,2231,6295,955

15,939

Bk 3912,213.3.93core

37,470,1021,130,081,1726,771,582,969,12100,38

5,9010,099

3,8240,1380,0100,0083,991

0,6953,5260,2111,5395,971

15,962

Bk 3913,213.3.93core

37,610,0521,010,061,2826,331,003,878,6599,87

5,9160,084

3,8110,1520,0070,0043,987

0,9073,4640,1331,4585,963

15,950

Bk 39123.3.92amph

37,040,0321,050,001,2426,350,523,718,9398,87

5,8870,113

3,8300,1490,0000,0033,993

0,8793,5020,0701,5215,972

15,964

Bk 39223.3.92amph

38,210,0121,610,040,5426,970,493,749,22100,83

5,9540,046

3,9230,0630,0050,0013,996

0,8693,5150,0651,5395,988

15,984

Bk 39323.3.92cpx (i)

36,930,0320,920,011,6727,080,723,688,2499,28

5,8590,141

3,7700,1990,0010,0033,989

0,8703,5920,0971,4015,960

15,949

Bk 39423.3.92cpx (i)

37,460,0421,260,001,0926,710,583,659,0199,80

5,9020,098

3,8510,1290,0000,0033,993

0,8573,5190,0771,5215,975

15,968

Bk 39523.3.92cpx (i)

37,080,0120,990,031,5125,450,483,949,4298,90

5,8740,126

3,7920,1790,0040,0013,989

0,9303,3710,0641,5995,964

15,954

Bk 391423.3.92cpx (i)

37,190,0521,350,031,2927,840,934,696,4299,79

5,8590,141

3,8230,1530,0040,0043,997

1,1013,6680,1241,0845,977

15,973

Bk 391523.3.92amph

36,740,0521,180,031,2626,810,563,608,6698,90

5,8510,149

3,8270,1510,0040,0043,998

0,8553,5720,0761,4785,979

15,977

Bk 391823.3.92cpx (i)

36,870,0321,260,031,6126,600,553,868,7199,52

5,8250,175

3,7830,1910,0040,0033,996

0,9093,5150,0741,4745,971

15,967

Bk 39224.6.92cpx (i)

37,370,0421,230,061,1725,240,324,818,7498,98

5,8900,110

3,8330,1390,0070,0033,993

1,1303,3260,0431,4765,975

15,968

Bk 39524.6.92amph

37,090,0121,040,001,3027,180,703,708,1899,20

5,8880,112

3,8240,1550,0000,0013,992

0,8753,6090,0941,3915,970

15,962

Bk 39724.6.92amph

36,820,0421,160,001,4329,500,693,286,9799,89

5,8470,153

3,8080,1710,0000,0033,997

0,7763,9180,0931,1865,973

15,970

Bk 39824.6.92cpx (i)

37,790,0521,560,030,8726,000,354,968,2699,87

5,9070,093

3,8790,1020,0040,0043,997

1,1563,3990,0461,3835,984

15,981

Bk 391224.6.92core

36,500,0620,730,021,3029,531,042,367,4498,98

5,8790,121

3,8140,1580,0030,0053,994

0,5673,9770,1421,2845,970

15,963

Bk 391324.6.92core

36,730,0321,190,081,1829,270,623,706,5599,36

5,8540,146

3,8340,1420,0100,0034,001

0,8793,9020,0841,1185,983

15,983

Bk 391424.6.92cpx (i)

36,640,0521,190,031,5429,280,753,526,7599,74

5,8220,178

3,7910,1840,0040,0043,999

0,8343,8900,1011,1495,974

15,973

Bk 395624.6.92cpx

37,690,0621,340,010,9125,240,464,938,6099,24

5,9200,080

3,8710,1080,0010,0053,993

1,1543,3150,0611,4475,978

15,971







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 395724.6.92cpx

37,090,0320,990,031,3526,190,533,569,2999,06

5,8850,115

3,8110,1610,0040,0033,991

0,8423,4750,0711,5795,968

15,958

Bk 395824.6.92cpx (i)

37,220,0421,110,010,8724,970,364,449,1498,16

5,9200,080

3,8780,1040,0010,0033,994

1,0533,3210,0491,5585,980

15,974

Bk 39428.1.93cpx (i)

36,600,0520,880,030,7828,001,292,008,9398,56

5,9120,088

3,8870,0950,0040,0043,998

0,4823,7820,1761,5455,985

15,983

Bk 39528.1.93cpx (i)

37,220,1020,830,001,8726,731,422,789,37100,33

5,8660,134

3,7350,2220,0000,0083,983

0,6533,5230,1901,5825,948

15,931

Bk 39728.1.93cpx (i)

37,150,0321,100,061,4027,731,033,657,7199,86

5,8720,128

3,8030,1670,0070,0033,993

0,8603,6650,1381,3065,969

15,962

Bk 39828.1.93cpx (i)

36,730,0820,990,071,8627,510,963,937,4299,56

5,8180,182

3,7360,2220,0090,0073,992

0,9283,6450,1291,2595,961

15,952

Bk 391228.1.93cpx (i)

37,240,0020,990,001,5227,370,943,857,7599,65

5,8850,115

3,7940,1800,0000,0003,989

0,9073,6160,1261,3125,961

15,950

Bk 391828.1.93cpx (i)

36,990,1921,190,001,2727,000,724,597,1799,12

5,8600,140

3,8160,1510,0000,0163,995

1,0843,5770,0971,2175,974

15,969

Bk 391928.1.93cpx (i)

37,090,2121,400,031,6026,560,625,257,0299,78

5,8150,185

3,7700,1890,0040,0183,995

1,2273,4820,0821,1795,971

15,966

Bk 392028.1.93cpx (i)

37,120,2521,170,001,1527,500,743,518,3099,74

5,8750,125

3,8250,1370,0000,0213,994

0,8283,6400,0991,4085,974

15,968

Bk 392328.1.93cpx (i)

37,410,0521,350,051,7027,040,685,047,01100,33

5,8390,161

3,7660,2000,0060,0043,992

1,1733,5300,0901,1725,964

15,956

Bk 393228.1.93cpx (i)

36,890,1720,760,002,1426,151,842,459,84100,23

5,8290,171

3,6940,2540,0000,0143,983

0,5773,4550,2461,6665,944

15,927

Bk 395328.1.93ab

37,340,0621,190,021,8426,240,503,639,62100,44

5,8410,159

3,7470,2170,0020,0053,988

0,8463,4320,0661,6125,957

15,945

Bk 395428.1.93ab

37,100,0020,950,001,7525,740,553,479,8399,40

5,8620,138

3,7630,2080,0000,0003,987

0,8173,4020,0741,6645,957

15,943

Bk 395828.1.93cpx

37,570,0821,320,002,0425,960,455,377,73100,52

5,8270,173

3,7240,2380,0000,0073,986

1,2413,3680,0591,2845,952

15,939

Bk 395928.1.93cpx

37,650,2621,240,341,5425,060,395,058,96100,49

5,8460,154

3,7330,1800,0420,0223,990

1,1693,2550,0511,4915,965

15,955

Bk 396228.1.93amph

37,100,1321,010,021,1424,690,374,778,8798,10

5,8960,104

3,8310,1360,0030,0113,991

1,1303,2820,0501,5105,972

15,963

Bk 396528.1.93core

36,970,0420,830,051,5527,301,502,678,7999,69

5,8770,123

3,7790,1850,0060,0033,989

0,6333,6290,2021,4975,961

15,949

Bk 396828.1.93core

37,150,0120,840,001,6527,171,243,028,7199,80

5,8830,117

3,7720,1970,0000,0013,986

0,7133,5980,1661,4785,955

15,941

Bk 391.4928.8.92cpx

37,150,0221,440,021,4226,360,514,198,6899,78

5,8400,160

3,8130,1680,0020,0023,997

0,9823,4650,0681,4625,977

15,974

Bk 391.5028.8.92cpx

37,150,0621,250,001,6325,820,493,769,6499,80

5,8410,159

3,7790,1930,0000,0053,992

0,8813,3960,0651,6245,966

15,958

Bk 391.5128.8.92cpx

37,370,0421,440,040,8126,140,483,759,4199,48

5,8990,101

3,8870,0970,0050,0033,999

0,8823,4500,0641,5915,988

15,988







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 391.5228.8.92cpx

37,130,0421,190,001,2125,900,543,759,3599,11

5,8810,119

3,8360,1440,0000,0033,994

0,8853,4310,0721,5875,975

15,969

Bk 391,14.5.92cpx

37,190,0421,090,011,0625,760,494,068,9898,69

5,9050,095

3,8520,1270,0010,0033,993

0,9613,4210,0661,5285,975

15,968

Bk 391,24.5.92cpx

37,110,0321,310,061,2126,360,504,078,6999,34

5,8630,137

3,8320,1440,0070,0033,997

0,9593,4830,0671,4715,979

15,977

Bk 392,14.5.92cpx

37,460,0421,340,041,1925,150,264,709,1399,31

5,8840,116

3,8350,1400,0050,0033,994

1,1003,3040,0351,5375,975

15,969

Bk 394,14.5.92cpx

37,610,0321,190,011,2124,850,254,719,3199,17

5,9090,091

3,8320,1430,0010,0033,989

1,1033,2650,0331,5675,969

15,958

Bk 395,14.5.92cpx

37,720,0521,200,021,4124,420,315,079,2499,44

5,8970,103

3,8020,1660,0020,0043,987

1,1813,1930,0411,5485,963

15,949

Bk 396,14.5.92cpx

37,790,0721,030,021,4824,130,315,099,3899,30

5,9110,089

3,7870,1740,0020,0063,982

1,1873,1560,0411,5725,955

15,938

Bk 397,14.5.92cpx

37,480,0421,170,071,3024,360,325,418,6598,80

5,8910,109

3,8130,1540,0090,0033,990

1,2673,2020,0431,4575,969

15,959

Bk 398,14.5.92cpx

37,640,0421,120,021,1825,910,425,107,7799,20

5,9190,081

3,8330,1400,0020,0033,988

1,1953,4070,0561,3095,967

15,956

Bk 399,14.5.92cpx

37,480,0821,040,011,4724,550,324,979,0598,97

5,8930,107

3,7920,1740,0010,0073,986

1,1653,2280,0431,5255,960

15,946

Bk 3910,14.5.92cpx (i)

36,980,0620,820,090,9926,820,583,478,6298,43

5,9190,081

3,8460,1200,0110,0053,982

1,8283,5890,0791,4785,974

15,966

Bk 3911,14.5.92core

36,360,0820,600,001,6228,101,272,498,1298,64

5,8580,142

3,7700,1960,0000,0073,990

0,5983,7870,1731,4025,960

15,950

Bk 3913,14.5.92core

36,610,0220,720,031,3230,001,152,047,4899,36

5,8870,113

3,8140,1590,0040,0023,993

0,4894,0340,1571,2895,968

15,961

Bk 3914,14.5.92core

36,770,0720,420,001,4130,011,012,117,3799,16

5,9190,081

3,7940,1700,0000,0063,985

0,5064,0400,1381,2715,955

15,940

Bk 3915,14.5.92core

36,370,0620,780,001,5730,350,842,506,8199,29

5,8460,154

3,7820,1900,0000,0053,994

0,5994,0800,1141,1735,966

15,960

Bk 3915,24.5.92cpx

37,480,0521,190,011,1924,760,415,108,6598,84

5,9010,099

3,8340,1410,0010,0043,990

1,1973,2600,0551,4595,971

15,961

Bk 3916,14.5.92core

36,790,0520,870,001,2529,820,503,136,7999,21

5,8880,112

3,8250,1510,0000,0043,993

0,7473,9910,0681,1645,970

15,964

Bk 3916,24.5.92cpx

37,850,0121,320,001,2824,320,285,289,1499,49

5,9060,094

3,8260,1510,0000,0013,988

1,2283,1740,0371,5285,967

15,955

Bk 39616.7.92cpx

37,380,1321,340,041,4725,080,794,908,5799,70

5,8520,148

3,7900,1730,0050,0113,992

1,1433,2830,1051,4385,969

15,961

Bk 7625.6.92core

36,990,0921,200,001,0828,290,743,038,2499,66

5,8790,121

3,8490,1290,0000,0083,997

0,7183,7590,1001,4035,980

15,977

Bk 7725.6.92core

37,150,0021,300,040,8927,920,653,817,6099,36

5,8960,104

3,8800,1060,0050,0003,999

0,9013,7050,0871,2925,986

15,986

Bk 7825.6.92core

37,520,0521,380,040,9727,310,405,186,6699,51

5,9000,100

3,8630,1150,0050,0043,996

1,2143,5910,0531,1225,981

15,977







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 7925.6.92core

37,240,0221,320,402,6226,580,565,836,73101,30

5,7400,260

3,6130,3040,0490,0023,991

1,3393,4270,0731,1115,951

15,942

Bk 71025.6.92core

37,650,0221,700,031,0027,360,565,835,89100,04

5,8760,124

3,8680,1180,0040,0024,000

1,3563,5710,0740,9855,986

15,986

Bk 71125.6.92amph

37,620,0221,820,010,9526,910,526,245,7599,85

5,8680,132

3,8790,1120,0010,0024,002

1,4513,5100,0690,9615,991

15,993

Bk 71225.6.92cpx

37,830,0121,370,000,9225,470,736,915,5398,77

5,9280,072

3,8750,1090,0000,0013,992

1,6143,3380,0970,9285,977

15,969

Bk 71325.6.92cpx

38,330,0422,120,130,8924,210,547,486,75100,49

5,8760,124

3,8730,1030,0160,0034,001

1,7093,1040,0701,1095,992

15,993

Bk 71425.6.92cpx

38,350,0321,800,020,4323,860,617,476,5499,11

5,9520,048

3,9390,0510,0020,0033,998

1,7283,0970,0801,0875,992

15,991

Bk 71525.6.92cpx

37,900,0121,630,010,5626,160,486,535,8399,12

5,9340,066

3,9260,0670,0010,0013,999

1,5243,4260,0640,9785,991

15,990

Bk 71625.6.92cpx

37,870,0221,400,000,6726,040,526,326,0398,88

5,9470,053

3,9070,0800,0000,0023,995

1,4793,4200,0691,0155,983

15,978

Bk 71725.6.92ap (i)

37,770,0521,680,021,2825,110,695,957,52100,07

5,8630,137

3,8290,1490,0020,0043,996

1,3773,2590,0911,2515,977

15,973

Bk 71925.6.92ap (i)

37,140,0521,100,011,0826,630,504,667,4598,62

5,8990,101

3,8490,1290,0010,0043,994

1,1033,5370,0671,2685,976

15,969

Bk 72025.6.92cpx (i)

37,570,0721,450,001,0426,660,565,217,0899,64

5,8920,108

3,8570,1230,0000,0063,996

1,2183,4970,0741,1905,979

15,975

Bk 72225.6.92amph (i)

37,600,0521,370,041,1727,520,574,527,38100,22

5,8900,110

3,8360,1380,0050,0043,994

1,0553,6050,0761,2395,975

15,969

Bk 72425.6.92amph

37,150,0321,250,020,7728,280,334,866,0398,73

5,9100,090

3,8940,0930,0030,0033,999

1,1523,7630,0441,0285,987

15,986

Bk 72525.6.92amph (i)

37,540,0821,460,011,1226,960,575,057,0999,88

5,8820,118

3,8450,1320,0010,0073,996

1,1793,5330,0761,1905,978

15,974

Bk 72625.6.92amph

37,800,0321,450,011,0328,720,434,596,55100,60

5,9080,092

3,8600,1210,0010,0033,994

1,0693,7540,0571,0975,977

15,971

Bk 72725.6.92cpx

37,190,0521,130,001,1629,480,383,626,8499,85

5,8930,107

3,8400,1380,0000,0043,994

0,8553,9060,0511,1615,974

15,968

Bk 72825.6.92cpx

37,090,0621,080,050,8928,880,573,507,1799,29

5,9100,090

3,8690,1070,0060,0053,996

0,8313,8490,0771,2245,981

15,977

Bk 72925.6.92amph

37,320,0621,150,011,0428,050,593,468,0699,73

5,9080,092

3,8540,1240,0010,0053,994

0,8163,7130,0791,3675,975

15,969

Bk 73025.6.92core

35,800,0621,020,001,9826,370,743,878,1297,96

5,7540,246

3,7360,2390,0000,0053,999

0,9273,5440,1011,3985,970

15,970

Bk 7126.4.93cpx

38,140,0521,990,050,6726,110,776,506,14100,42

5,9000,100

3,9090,0780,0060,0044,002

1,4993,3780,1011,0185,995

15,997

Bk 7426.4.93cpx

38,570,0021,990,010,5524,780,577,076,69100,22

5,9390,061

3,9300,0630,0010,0003,999

1,6233,1910,0741,1045,991

15,990

Bk 72526.4.93phe (i)

37,350,0521,330,020,9225,910,554,268,7699,15

5,9010,099

3,8720,1100,0020,0043,997

1,0033,4230,0741,4835,983

15,979







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 72726.4.93phe (i)

37,640,0621,250,001,1924,881,134,628,7899,55

5,9050,095

3,8340,1410,0000,0053,990

1,0803,2630,1501,4765,970

15,960

Bk 72826.4.93amph (i)

37,650,1121,410,000,8924,831,084,608,9299,49

5,9110,089

3,8730,1050,0000,0093,994

1,0763,2600,1441,5005,981

15,975

Bk 73926.4.93cpx (i)

37,780,2121,400,051,0224,560,704,859,2499,80

5,9010,099

3,8400,1190,0060,0183,992

1,1293,2080,0931,5465,976

15,968

Bk 74326.4.93cpx (i)

38,060,1421,390,030,7924,640,674,999,0399,74

5,9410,059

3,8770,0920,0040,0123,991

1,1613,2170,0891,5105,977

15,968

Bk 74426.4.93cpx (i)

38,250,0421,660,050,4824,820,766,267,2399,55

5,9540,046

3,9280,0560,0060,0033,997

1,4523,2310,1001,2065,990

15,987

Bk 76526.4.93phe (i)

37,410,0421,320,061,3125,930,714,478,5099,75

5,8720,128

3,8160,1550,0070,0033,994

1,0463,4030,0941,4295,973

15,967

Bk 7227.8.91amph

37,230,0621,710,041,0426,200,565,656,8799,35

5,8450,155

3,8620,1230,0050,0054,004

1,3223,4390,0741,1565,992

15,995

Bk 7327.8.91amph

37,360,0021,840,060,5226,100,856,106,0798,90

5,8830,117

3,9350,0610,0070,0004,009

1,4323,4370,1131,0246,006

16,015

Bk 7427.8.91core

37,710,0421,960,001,3225,580,726,107,10100,53

5,8300,170

3,8320,1540,0000,0034,000

1,4063,3080,0941,1765,984

15,984

Bk 7527.8.91amph

37,230,1021,110,031,7524,880,924,069,6299,70

5,8470,153

3,7540,2060,0040,0083,988

0,9503,2670,1221,6195,959

15,946

Bk 712,14.5.92core

36,590,0920,470,031,7728,681,102,148,3899,25

5,8710,129

3,7420,2130,0040,0083,985

0,5123,8480,1491,4415,950

15,935

Bk 7216.7.92core

37,330,0321,300,041,3428,450,394,706,4099,98

5,8690,131

3,8160,1580,0050,0033,995

1,1013,7410,0521,0785,973

15,967

Bk 7226.7.92cpx

38,210,0221,650,010,9124,920,727,655,3499,43

5,9220,078

3,8770,1060,0010,0023,994

1,7673,2310,0950,8875,979

15,973

k 7246.7.92amph

37,980,0821,420,030,9124,200,476,797,0498,92

5,9270,073

3,8660,1070,0040,0073,992

1,5793,1580,0621,1775,976

15,968

Bk 7266.7.92amph

37,280,0421,130,001,1727,860,543,987,5299,52

5,8990,101

3,8390,1390,0000,0033,993

0,9393,6860,0721,2755,972

15,965

Bk 7276.7.92core

36,900,0820,890,021,6326,960,732,789,5499,53

5,8600,140

3,7700,1950,0030,0073,989

0,6583,5810,0981,6235,960

15,949

Bk 7286.7.92core

36,670,0820,700,021,5328,130,802,438,7799,13

5,8730,127

3,7800,1850,0030,0073,989

0,5803,7670,1091,5055,961

15,950

Bk 7296.7.92ab

37,930,0821,120,000,7427,530,843,148,90100,27

5,9700,030

3,8880,0870,0000,0073,989

0,7373,6240,1121,5015,973

15,962

Bk 7316.7.92amph

36,510,0620,970,031,5127,580,852,858,6999,05

5,8380,162

3,7900,1820,0040,0053,995

0,6793,6880,1151,4895,971

15,966

Bk 7366.7.92amph

37,100,0421,040,031,0227,540,623,588,0799,04

5,9070,093

3,8550,1230,0040,0033,994

0,8503,6670,0841,3775,977

15,971

Bk 7386.7.92amph

37,160,1121,270,021,4026,240,754,637,8699,44

5,8550,145

3,8040,1650,0020,0093,994

1,0873,4580,1001,3275,972

15,966

Bk 7466.7.92cpx (i)

36,750,9920,400,001,4822,961,125,028,9997,71

5,8640,136

3,7010,1780,0000,0853,976

1,1943,0630,1511,5375,946

15,922







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 7486.7.92cpx (i)

37,470,1021,210,131,0824,301,045,088,5899,00

5,8970,103

3,8310,1280,0160,0083,993

1,1923,1990,1391,4475,976

15,968

Bk 7496.7.92cpx (i)

37,700,0721,360,061,0024,940,954,828,6799,57

5,9090,091

3,8540,1170,0070,0063,993

1,1263,2690,1261,4565,977

15,971

Bk 7516.7.92amph

37,120,0321,340,020,9627,700,434,816,5999,00

5,8840,116

3,8710,1140,0030,0033,999

1,1363,6720,0581,1195,986

15,985

Bk 7526.7.92gl (i)

37,450,0421,400,050,8825,740,804,538,4299,31

5,9020,098

3,8760,1040,0060,0033,997

1,0643,3920,1071,4225,985

15,982

Bk 7536.7.92amph (i)

37,310,0521,290,041,1325,190,794,878,3198,98

5,8840,116

3,8420,1340,0050,0043,995

1,1453,3230,1061,4045,978

15,972

Bk 7576.7.92cpx

37,220,0221,320,060,8628,130,454,586,5899,22

5,8980,102

3,8800,1020,0080,0023,999

1,0823,7270,0601,1175,987

15,986

Bk 7586.7.92core

37,410,0921,110,031,2625,711,353,828,8999,68

5,8960,104

3,8170,1500,0040,0083,990

0,8973,3890,1801,5015,968

15,958

Bk 7596.7.92core

37,020,0921,100,021,6426,121,693,089,25100,00

5,8450,155

3,7710,1950,0020,0083,991

0,7253,4480,2261,5655,964

15,955

Bk 7606.7.92core

36,920,1021,120,001,4226,111,203,668,7299,25

5,8550,145

3,8020,1700,0000,0093,993

0,8653,4630,1611,4825,971

15,964

Bk 7626.7.92core

37,140,1221,170,001,4425,710,794,238,7299,32

5,8610,139

3,7980,1710,0000,0103,992

0,9953,3930,1061,4745,968

15,960

Bk 7636.7.92qtz

37,720,0321,520,020,8824,590,586,327,2198,87

5,9080,092

3,8810,1030,0020,0033,996

1,4753,2210,0771,2105,984

15,980

Bk 7656.7.92cpx (i)

38,170,0021,160,070,8927,350,694,567,40100,29

5,9670,033

3,8660,1050,0090,0003,987

1,0633,5760,0911,2395,969

15,956

Bk 7666.7.92cpx

37,610,0221,340,071,1026,240,805,836,3499,35

5,8990,101

3,8440,1300,0090,0023,994

1,3633,4410,1061,0655,976

15,970

Bk 7676.7.92cpx

37,560,0121,400,010,7525,760,536,266,2098,48

5,9220,078

3,8990,0890,0010,0013,997

1,4713,3960,0711,0475,986

15,983

Bk 787.7.92cpx

37,560,0321,600,001,0424,790,586,007,5299,12

5,8790,121

3,8640,1220,0000,0033,998

1,4003,2460,0771,2615,984

15,981

Bk 797.7.92amph

37,640,0321,610,040,9124,450,566,417,2698,91

5,8900,110

3,8760,1070,0050,0033,998

1,4953,2000,0741,2175,987

15,985

Bk 7197.7.92amph

37,680,0221,680,030,6625,260,596,037,1199,07

5,9070,093

3,9120,0780,0040,0024,001

1,4093,3120,0781,1945,994

15,995

Bk 7227.7.92cpx (i)

37,320,0221,550,070,9526,510,636,325,5498,90

5,8730,127

3,8700,1120,0090,0024,001

1,4823,4890,0840,9345,989

15,990

Bk 7237.7.92cpx (i)

37,180,0421,560,011,2626,700,525,756,2999,31

5,8420,158

3,8350,1490,0010,0034,000

1,3473,5080,0691,0595,983

15,983

Bk 7257.7.92cpx (i)

37,160,0521,220,141,0525,310,555,267,7698,51

5,8820,118

3,8400,1250,0180,0043,997

1,2413,3510,0741,3165,981

15,978

Bk 7267.7.92cpx (i)

37,100,0121,500,061,4225,300,725,197,9899,28

5,8290,171

3,8110,1680,0070,0013,999

1,2153,3250,0961,3435,980

15,978

Bk 7307.7.92cpx (i)

37,370,0121,390,000,9525,760,585,247,5398,84

5,8970,103

3,8750,1130,0000,0013,997

1,2323,4000,0781,2735,983

15,980







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 7317.7.92cpx (i)

37,200,0021,430,031,3125,540,635,357,5999,08

5,8530,147

3,8270,1550,0040,0003,997

1,2553,3600,0841,2795,979

15,976

Bk 7337.7.92amph

36,900,0621,260,081,2225,850,704,448,2998,80

5,8520,148

3,8260,1460,0100,0053,998

1,0503,4290,0941,4095,981

15,979

Bk 7347.7.92ab

36,980,1521,230,001,6324,780,924,169,4899,32

5,8290,171

3,7730,1930,0000,0133,992

0,9773,2660,1231,6015,967

15,960

Bk 7357.7.92core

37,490,0521,540,041,1323,410,804,919,9299,29

5,8700,130

3,8450,1340,0050,0043,997

1,1463,0650,1061,6645,981

15,978

Bk 7367.7.92core

37,500,0721,290,051,6124,070,875,258,8699,57

5,8560,144

3,7750,1890,0060,0063,989

1,2223,1440,1151,4825,964

15,953

Bk 7377.7.92amph

37,590,0421,440,030,8726,750,525,995,9199,15

5,9070,093

3,8790,1030,0040,0033,997

1,4033,5160,0690,9955,984

15,980

Bk 7477.7.92cpx (i)

37,560,0621,290,050,2724,171,852,8710,9099,03

5,9660,034

3,9520,0330,0060,0053,999

0,6803,2110,2491,8555,995

15,994

Bk 7487.7.92cpx (i)

37,420,1021,210,001,3824,340,994,0010,1099,54

5,8790,121

3,8070,1630,0000,0083,990

0,9373,1980,1321,7005,967

15,957

Bk 7517.7.92cpx (i)

37,380,0321,230,031,1826,841,364,756,7499,54

5,8920,108

3,8360,1400,0040,0033,993

1,1163,5380,1821,1385,974

15,967

Bk 7617.7.92core

37,010,1421,150,001,4224,520,993,6010,2999,12

5,8550,145

3,7990,1690,0000,0123,992

0,8493,2440,1331,7445,970

15,962

Bk 7737.7.92amph

37,330,0321,180,020,9526,670,634,208,0799,07

5,9130,087

3,8680,1130,0030,0033,994

0,9923,5330,0851,3705,979

15,973

Bk 83014.3.93amph

38,180,0021,700,001,5025,260,517,695,40100,24

5,8710,129

3,8040,1740,0000,0003,991

1,7633,2480,0660,8905,967

15,957

Bk 83114.3.93amph

37,840,0721,720,001,0527,200,786,534,99100,19

5,8810,119

3,8590,1230,0000,0063,998

1,5133,5360,1030,8315,982

15,980

Bk 83214.3.93cpx

37,840,3521,650,000,8526,000,646,196,47100,00

5,8890,111

3,8600,1000,0000,0293,996

1,4363,3840,0841,0795,983

15,979

Bk 83314.3.93cpx

37,770,0921,670,001,0125,340,506,566,5499,48

5,8840,116

3,8630,1180,0000,0083,997

1,5233,3020,0661,0925,983

15,980

Bk 83414.3.93cpx

37,910,0121,440,031,0524,610,516,547,0499,13

5,9140,086

3,8560,1230,0040,0013,992

1,5213,2100,0671,1775,975

15,967

Bk 83514.3.93cpx

38,110,0021,740,000,9925,070,576,477,0299,97

5,9030,097

3,8720,1150,0000,0003,995

1,4943,2470,0751,1655,981

15,976

Bk 85114.3.93amph

38,380,0221,710,001,1825,490,497,225,90100,39

5,9050,095

3,8430,1370,0000,0023,991

1,6563,2790,0640,9735,972

15,963

Bk 85214.3.93core

37,900,0721,640,021,1927,370,336,285,59100,40

5,8800,120

3,8360,1400,0020,0063,995

1,4523,5520,0430,9295,976

15,971

Bk 85314.3.93core

37,240,0121,490,031,3629,790,283,906,65100,75

5,8450,155

3,8210,1600,0040,0013,999

0,9123,9100,0371,1185,978

15,978

Bk 85414.3.93core

37,360,0320,950,011,1728,880,672,957,9699,99

5,9210,079

3,8340,1400,0010,0033,989

0,6973,8280,0901,3525,967

15,956

Bk 85514.3.93core

37,110,1020,550,011,8628,661,112,248,60100,24

5,8870,113

3,7300,2220,0010,0093,981

0,5303,8020,1491,4625,943

15,923







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Bk 81029.1.93ap

38,130,0122,020,001,1725,010,408,245,02100,00

5,8630,137

3,8530,1350,0000,0013,998

1,8883,2160,0520,8275,983

15,982

Bk 81129.1.93cpx

37,890,0022,030,001,2924,700,558,125,2399,81

5,8390,161

3,8400,1490,0000,0004,000

1,8653,1840,0720,8645,984

15,984

Bk 81529.1.93core

37,240,0721,130,041,6225,701,463,828,8699,94

5,8560,144

3,7720,1920,0050,0063,989

0,8953,3800,1941,4935,963

15,952

Bk 81729.1.93core

36,860,1920,780,031,1926,850,703,059,0698,71

5,8970,103

3,8160,1430,0040,0163,990

0,7273,5930,0951,5535,968

15,958

Bk 81829.1.93core

36,680,2820,970,191,7127,311,152,918,87100,07

5,8100,190

3,7250,2040,0240,0243,993

0,6873,6180,1541,5055,965

15,958

Bk 81929.1.93cpx (i)

37,230,0021,270,001,6125,041,523,719,5499,91

5,8490,151

3,7880,1900,0000,0003,992

0,8693,2900,2021,6065,967

15,958

Bk 82429.1.93cpx (i)

37,310,1321,180,001,3825,381,533,429,6099,93

5,8740,126

3,8040,1630,0000,0113,990

0,8033,3420,2041,6195,968

15,958

Bk 82529.1.93core

37,510,1221,240,001,4824,541,194,589,0999,75

5,8720,128

3,7920,1740,0000,0103,988

1,0693,2130,1581,5255,964

15,952

Bk 9162.7.94amph

37,580,0521,310,050,9827,810,684,047,62100,12

5,9090,091

3,8590,1160,0060,0043,995

0,9473,6570,0911,2845,978

15,973

Bk 9172.7.94chl

37,580,1020,890,021,2524,332,741,6911,75100,35

5,9290,071

3,8140,1480,0020,0083,984

0,3973,2100,3661,9865,960

15,944

Bk 9182.7.94core

37,750,1020,770,081,0320,466,012,5410,9599,69

5,9650,035

3,8330,1220,0100,0083,981

0,5982,7040,8041,8545,961

15,942

Bk 9192.7.94core

37,830,2420,940,071,0120,564,153,1811,6599,63

5,9470,053

3,8270,1190,0090,0203,983

0,7452,7030,5531,9625,963

15,946

Bk 9202.7.94chl

38,330,0321,650,020,4827,060,505,856,28100,20

5,9620,038

3,9300,0570,0020,0033,996

1,3563,5190,0661,0475,988

15,984

Cig 90/40461.6.91core

37,080,0920,940,011,5928,460,533,018,32100,03

5,8690,131

3,7760,1890,0010,0083,989

0,7103,7680,0711,4115,960

15,949

Cig 90/40471.6.91core

37,090,1220,980,001,7929,510,513,017,63100,64

5,8480,152

3,7470,2130,0000,0103,989

0,7073,8910,0681,2895,956

15,944

Cig 90/40481.6.91cpx

37,370,0521,330,021,4227,450,915,355,9399,83

5,8630,137

3,8060,1670,0020,0043,994

1,2513,6020,1210,9975,971

15,964

Cig 90/40491.6.91core

36,820,0720,910,001,6429,340,572,707,8999,93

5,8540,146

3,7720,1960,0000,0063,991

0,6403,9010,0771,3445,962

15,953

Cig 90/40501.6.91core

36,940,1120,970,021,1628,430,623,028,0899,35

5,8900,110

3,8310,1390,0030,0093,993

0,7183,7910,0841,3805,973

15,966

Cig 90/40561.6.91core

37,740,0321,450,031,2027,410,924,946,73100,45

5,8900,110

3,8360,1410,0040,0033,994

1,1493,5780,1221,1255,974

15,968

Cig 90/40571.6.91core

37,210,0821,040,001,6426,060,782,8510,37100,03

5,8640,136

3,7720,1950,0000,0073,988

0,6693,4350,1041,7515,959

15,947

Cig 90/4011.6.91acore

37,000,1120,850,051,2428,910,512,887,9799,52

5,8970,103

3,8130,1490,0060,0093,991

0,6843,8530,0691,3615,967

15,958

Cig 90/4021.6.91acore

37,240,0820,880,041,6129,190,522,937,93100,42

5,8810,119

3,7670,1920,0050,0073,987

0,6903,8550,0701,3425,956

15,943





Cig 90/4051.6.91acore

37,040,1020,840,001,5029,040,523,017,7599,80

5,8840,116

3,7850,1790,0000,0093,988

0,7133,8580,0701,3195,960

15,948



SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Cig 90/4011.6.91bcore

37,350,0921,020,021,0129,140,532,927,93100,01

5,9220,078

3,8500,1210,0030,0083,992

0,6903,8640,0711,3475,972

15,964

Cig 90/4041.6.91bcore

37,010,0920,920,001,4627,890,593,378,1299,46

5,8770,123

3,7930,1750,0000,0083,990

0,7983,7050,0791,3825,963

15,953

Cig 90/4081.6.91bcpx

37,490,0321,180,021,1627,250,745,425,9899,28

5,9060,094

3,8380,1380,0020,0033,992

1,2733,5910,0991,0095,971

15,963

Cig 91-11016.6.93cpx

38,540,0121,920,020,8226,250,357,704,87100,48

5,9220,078

3,8910,0950,0020,0013,996

1,7633,3730,0460,8025,984

15,980

Cig 91-11116.6.93cpx

38,580,0221,930,020,9026,020,297,834,97100,56

5,9170,083

3,8800,1030,0020,0023,995

1,7903,3380,0380,8175,982

15,977

Cig 91-11416.6.93cz

38,070,0521,600,021,1225,041,265,697,52100,37

5,9010,099

3,8460,1300,0020,0043,993

1,3153,2460,1651,2495,975

15,967

Cig 91-11716.6.93gl

38,570,0421,710,021,2126,630,367,125,37101,03

5,9120,088

3,8340,1400,0020,0033,990

1,6273,4140,0470,8825,969

15,958

Cig 91-11816.6.93gl

38,200,0521,530,001,4926,830,326,835,41100,66

5,8870,113

3,7980,1730,0000,0043,988

1,5693,4580,0420,8935,962

15,951

Cig 91-11916.6.93biot

38,340,0621,630,030,7827,860,445,945,68100,76

5,9380,062

3,8870,0910,0040,0053,994

1,3713,6080,0580,9435,980

15,974

Cig 91-12016.6.93biot

38,200,0121,730,011,3427,970,496,025,61101,37

5,8810,119

3,8240,1550,0010,0013,993

1,3813,6010,0640,9255,971

15,965

Cig 91-12116.6.93biot

38,220,0321,670,020,9328,070,465,895,57100,86

5,9180,082

3,8730,1080,0020,0023,995

1,3593,6350,0600,9245,979

15,974

Cig 91-12216.6.93biot

38,330,0021,760,001,1428,260,425,875,66101,44

5,9020,098

3,8510,1330,0000,0003,994

1,3473,6390,0550,9345,975

15,969

Cig 91-12416.6.93qtz (i)

38,240,0321,640,001,1426,640,776,106,20100,76

5,9070,093

3,8460,1330,0000,0023,992

1,4043,4420,1011,0265,973

15,965

Cig 91-12516.6.93qtz (i)

38,120,0221,500,000,7328,540,595,465,44100,40

5,9470,053

3,9000,0860,0000,0023,994

1,2703,7240,0780,9095,981

15,975

Cig 91-12616.6.93gl

38,770,0221,950,001,2325,260,288,285,16100,95

5,9010,099

3,8380,1410,0000,0023,991

1,8783,2160,0360,8415,971

15,962

Cig 91-12716.6.93gl

38,900,0522,090,020,9824,930,258,684,99100,89

5,9120,088

3,8680,1120,0020,0043,994

1,9663,1680,0320,8125,979

15,973

Cig 91-12816.6.93gl

38,840,0521,910,000,5926,590,507,594,71100,78

5,9570,043

3,9170,0680,0000,0043,994

1,7353,4100,0650,7745,984

15,979

Cig 91-12916.6.93gl

38,970,0122,100,051,0125,570,348,285,03101,36

5,9120,088

3,8640,1150,0060,0013,994

1,8723,2450,0440,8185,979

15,972

Cig 91-13816.6.93biot

39,420,0022,370,030,5724,270,249,484,73101,11

5,9470,053

3,9250,0640,0040,0003,997

2,1323,0620,0310,7655,989

15,986

Cig 91-13916.6.93cpx (i)

39,100,0422,510,000,5624,140,179,594,67100,78

5,9160,084

3,9310,0640,0000,0034,002

2,1633,0540,0220,7575,996

15,998

Cig 91-14016.6.93biot

39,310,0022,050,050,7625,960,258,434,64101,46

5,9560,044

3,8930,0870,0060,0003,992

1,9043,2900,0320,7535,979

15,970







SiAlt

AloFe3CrTi

MgFe2MnCa

sum



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Cig 91-14116.6.93biot

38,830,0421,960,001,0225,570,248,414,74100,81

5,9190,081

3,8640,1170,0000,0033,992

1,9113,2600,0310,7745,976

15,968

Cig 91-14216.6.93biot

38,750,0422,200,030,9025,430,398,334,96101,03

5,8980,102

3,8810,1030,0040,0033,998

1,8903,2370,0500,8095,986

15,984

Cig 91-14316.6.93biot

38,600,0221,990,020,9926,570,637,075,42101,31

5,9050,095

3,8690,1140,0020,0023,996

1,6123,3990,0820,8885,981

15,976

Cig 91-14416.6.93cpx (i)

38,860,0222,230,021,0425,170,328,884,57101,10

5,8930,107

3,8660,1180,0020,0023,996

2,0073,1910,0410,7425,982

15,978

Cig 91-14516.6.93core

38,860,0721,890,021,0727,050,257,305,12101,64

5,9200,080

3,8500,1230,0020,0063,991

1,6583,4470,0320,8365,972

15,963

Cig 91-14616.6.93cpx (i)

39,050,2522,130,030,7024,830,228,894,87100,97

5,9270,073

3,8850,0800,0040,0203,994

2,0113,1520,0280,7925,983

15,978

Cig 91-14716.6.93biot

38,740,0121,880,011,3926,150,217,865,09101,34

5,8940,106

3,8170,1590,0010,0013,990

1,7823,3280,0270,8305,967

15,956

Cig 91-14816.6.93biot

38,590,0221,930,061,2626,280,227,745,10101,20

5,8860,114

3,8290,1450,0070,0023,993

1,7603,3520,0280,8345,974

15,967

Cig 91-14916.6.93biot

38,960,0121,940,000,5125,910,287,875,07100,55

5,9690,031

3,9310,0590,0000,0013,994

1,7973,3200,0360,8325,985

15,980

Cig 91-14817.6.93biot

38,930,0122,180,000,7424,420,248,915,06100,49

5,9260,074

3,9050,0850,0000,0013,997

2,0223,1090,0310,8255,986

15,983

Cig 91-14917.6.93biot

38,970,0322,140,001,0024,730,238,904,92100,92

5,9110,089

3,8690,1140,0000,0023,994

2,0123,1370,0300,8005,979

15,972

Cig 91-15017.6.93biot

39,180,1322,330,280,4525,220,268,804,89101,53

5,9240,076

3,9030,0510,0330,0114,002

1,9833,1890,0330,7925,997

15,999

Cig 91-15117.6.93biot

38,820,0021,870,000,9225,450,348,254,86100,51

5,9370,063

3,8780,1060,0000,0003,992

1,8813,2550,0440,7965,976

15,968

Cig 91-15217.6.93biot

38,620,1121,900,000,4926,990,606,815,27100,79

5,9500,050

3,9260,0570,0000,0093,997

1,5643,4770,0780,8705,989

15,986

Cig 91-15317.6.93core

38,240,0321,450,001,2427,240,446,275,65100,55

5,9180,082

3,8300,1440,0000,0023,988

1,4463,5250,0580,9375,966

15,954

Cig 91-15417.6.93core

38,830,0021,590,021,1326,140,307,645,08100,73

5,9470,053

3,8430,1300,0020,0003,986

1,7443,3480,0390,8345,964

15,950

Cig 91-15917.6.93core

37,940,1221,080,051,2026,031,414,487,92100,23

5,9320,068

3,8170,1410,0060,0103,985

1,0443,4040,1871,3275,961

15,946

Cig 91-16017.6.93core

38,130,0421,140,021,3825,791,145,047,71100,39

5,9290,071

3,8030,1620,0020,0033,983

1,1683,3530,1501,2855,956

15,939

Cig 91-16117.6.93core

38,250,0721,190,041,1625,111,205,287,90100,21

5,9450,055

3,8270,1360,0050,0063,984

1,2233,2640,1581,3165,961

15,945

Cig 91-16217.6.93core

38,330,0821,370,001,6025,540,955,997,08100,94

5,9000,100

3,7770,1850,0000,0073,983

1,3743,2880,1241,1685,954

15,937

Cig 91-16317.6.93core

38,500,0721,220,031,3425,060,885,787,70100,58

5,9430,057

3,8040,1560,0040,0063,981

1,3303,2360,1151,2745,954

15,935

Cig 91-16717.6.93phe(i)

38,290,0121,480,001,4827,090,835,276,97101,42

5,9000,100

3,8010,1710,0000,0013,987

1,2103,4910,1081,1515,960

15,947

C-26 Appendix C Table C4/C5 garnet/glaucophane



sampleanalysedateposition

SiO2TiO2Al2O3Cr2O3Fe2O3FeOMnOMgOCaOZnONa2OK2O

H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

Bk 392724.6.92core

56,290,0511,310,042,087,980,0710,361,33n.a6,850,02

2,1598,53

7,8330,1678,000

1,6880,2180,0040,0042,1490,9280,008 -5,000

0,1981,8022,000

0,0470,0040,050

15,050

2

Bk 392824.6.92core

55,930,0211,280,042,677,480,0310,421,22n.a6,880,03

2,1598,14

7,8110,1898,000

1,6680,2810,0040,0012,1690,8730,004 -5,000

0,1831,8172,000

0,0450,0050,051

15,051

2

Bk 393924.6.92core

56,100,0311,240,022,727,040,0710,501,04n.a6,870,02

2,1597,80

7,8400,1608,000

1,6910,2860,0020,0022,1870,8230,008 -5,000

0,1561,8442,000

0,0170,0040,021

15,021

2

Bk 394124.6.92core

56,720,0511,640,073,885,450,0710,931,00n.a6,600,02

2,1898,60

7,8150,1858,000

1,7060,4020,0080,0042,2450,6280,008 -5,000

0,1481,7632,000

0,0000,0040,004

15,004

2

Bk 394427.8.92rim

58,170,0311,580,001,846,870,0411,191,190,126,880,03

2,21100,15

7,8960,1048,000

1,7490,1880,0000,0022,2640,7800,0050,0125,000

0,1731,8112,000

0,0000,0050,005

15,005

2

Bk 39443.7.94core

57,580,0611,540,003,306,800,0010,981,240,106,920,03

2,21100,76

7,8120,1888,000

1,6570,3370,0000,0042,2200,7720,0000,0105,000

0,1801,8202,000

0,0000,0050,006

15,006

2

Bk 39453.7.94core

56,910,0411,410,001,947,720,0410,391,100,106,840,04

2,1798,69

7,8800,1208,000

1,7420,2020,0000,0032,1440,8940,0050,0105,000

0,1631,8362,000

0,0000,0070,007

15,007

2

Bk 3915.5.92core

55,490,0211,040,000,699,870,099,801,60n.a6,950,04

2,1297,71

7,8440,1568,000

1,6830,0740,0000,0022,0651,1660,011 -5,000

0,2421,7582,000

0,1470,0070,154

15,154

2

Bk 3925.5.92core

56,680,0411,410,021,398,750,0210,181,17n.a7,090,01

2,1698,92

7,8620,1388,000

1,7280,1450,0020,0032,1051,0150,002 -5,000

0,1741,8262,000

0,0810,0020,083

15,083

2

Bk 7432.7.94core

57,610,0211,710,071,356,250,0211,721,450,176,910,03

2,2099,50

7,8560,1448,000

1,7390,1380,0080,0012,3820,7120,0020,0175,000

0,2121,7882,000

0,0390,0050,044

15,044

2

Bk 7442.7.94core

57,370,0211,900,022,205,960,0011,381,290,296,840,03

2,2099,50

7,8310,1698,000

1,7450,2260,0020,0012,3150,6810,0000,0295,000

0,1891,8102,000

0,0000,0050,005

15,005

2



SiAlt

AloFe3CrTi

MgFe2MnCa

sum

Cig 91-18317.6.93biot

38,840,0122,010,000,9825,790,188,204,93100,94

5,9190,081

3,8730,1120,0000,0013,993

1,8633,2870,0230,8055,978

15,971

Cig 91-18417.6.93biot

38,680,0421,860,041,1625,790,277,985,06100,88

5,9070,093

3,8410,1330,0050,0033,991

1,8163,2940,0350,8285,973

15,964

Cig 91-18517.6.93core

38,410,0321,840,001,1228,570,346,155,19101,65

5,8990,101

3,8520,1290,0000,0023,994

1,4083,6700,0440,8545,976

15,971

Cig 91-18617.6.93core

38,290,0421,200,001,5426,141,135,257,32100,91

5,9210,079

3,7850,1800,0000,0033,981

1,2103,3810,1481,2135,952

15,933

Cig 91-18717.6.93core

38,220,1421,500,010,7128,071,274,966,05100,93

5,9470,053

3,8900,0830,0010,0123,993

1,1503,6530,1671,0095,979

15,972

Cig 91-1528.11.93core

38,820,3321,910,010,4726,010,337,914,88100,67

5,9500,050

3,9080,0540,0010,0273,994

1,8073,3340,0430,8015,985

15,980

position means analysis of: core is core position in a gln grain, rim is rim position in a gln grain

normed on 23 oxygen, Fe3 over Si+Ti+Al+Fe+Mn+Mg+Ca+Zn = 15

C-27Appendix C Table C5 glaucophane



H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH




H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH


Bk 7452.7.94core

56,680,0311,870,072,846,690,0010,801,240,266,970,03

2,1999,66

7,7760,2248,000

1,6950,2930,0080,0022,2080,7670,0000,0265,000

0,1821,8182,000

0,0360,0050,042

15,042

2

Bk 71426.4.93rim

57,150,0811,720,121,306,450,0611,491,540,196,810,04

2,1999,14

7,8380,1628,000

1,7320,1350,0130,0062,3490,7390,0070,0195,000

0,2261,7742,000

0,0370,0070,044

15,044

2

Bk 7197.8.92core

57,130,0011,820,011,965,930,0011,180,910,236,950,03

2,1898,33

7,8720,1288,000

1,7920,2040,0010,0002,2960,6840,0000,0235,000

0,1341,8572,000

0,0000,0050,005

15,005

2

Bk 7237.8.92rim

56,060,0311,700,002,027,220,0510,541,400,246,760,04

2,1598,22

7,8070,1938,000

1,7270,2120,0000,0022,1880,8410,0060,0255,000

0,2091,7912,000

0,0340,0070,041

15,041

2

Bk 7247.8.92core

56,840,0411,660,002,406,830,0510,781,370,236,690,04

2,1899,11

7,8270,1738,000

1,7200,2490,0000,0032,2130,7860,0060,0235,000

0,2021,7862,000

0,0000,0070,007

15,007

2

Bk 7257.8.92rim

55,950,0211,740,002,477,520,0310,391,570,286,730,05

2,1698,91

7,7660,2348,000

1,6860,2580,0000,0012,1490,8730,0040,0295,000

0,2331,7672,000

0,0450,0090,054

15,054

2

Bk 7297.8.92rim

55,260,0711,620,002,147,000,0711,082,390,176,310,05

2,1598,31

7,7110,2898,000

1,6220,2250,0000,0052,3050,8170,0080,0185,000

0,3571,6432,000

0,0650,0090,074

15,074

2

Bk 7317.8.92rim

56,570,0311,860,012,996,130,0810,731,280,236,550,03

2,1798,66

7,8090,1918,000

1,7380,3110,0010,0022,2080,7070,0090,0235,000

0,1891,7532,000

0,0000,0050,005

15,005

2

Bk 7447.8.92core

55,830,0211,860,033,556,660,0910,571,660,216,570,06

2,1799,29

7,7150,2858,000

1,6470,3690,0030,0012,1770,7700,0110,0215,000

0,2461,7542,000

0,0060,0110,017

15,017

2

Bk 7467.8.92core

56,900,0011,810,042,955,700,0311,191,240,206,700,04

2,1898,98

7,8120,1888,000

1,7230,3050,0040,0002,2900,6540,0030,0205,000

0,1821,7842,000

0,0000,0070,007

15,007

2

Bk 81429.1.93bcore

57,500,1511,720,002,694,320,0012,080,690,197,160,05

2,2098,74

7,8540,1468,000

1,7410,2770,0000,0112,4590,4930,0000,0195,000

0,1011,8962,000

0,0000,0090,009

15,009

2

Bk 81529.1.93brim

57,150,0311,810,002,405,750,0411,511,360,216,800,05

2,1999,30

7,8170,1838,000

1,7210,2470,0000,0022,3470,6570,0050,0215,000

0,1991,8012,000

0,0030,0090,012

15,012

2

Bk 81729.1.93brim

56,630,0311,590,032,617,020,0810,351,070,266,740,06

2,1698,63

7,8450,1558,000

1,7370,2720,0030,0022,1370,8130,0090,0275,000

0,1591,8102,000

0,0000,0110,011

15,011

2

Bk 81829.1.93bcore

56,860,0211,920,041,586,600,0110,910,870,307,170,06

2,1798,52

7,8500,1508,000

1,7900,1650,0040,0012,2450,7630,0010,0315,000

0,1291,8712,000

0,0480,0110,059

15,059

2

Bk 82029.1.93brim

57,050,0311,630,032,806,720,0110,560,890,226,890,04

2,1899,05

7,8540,1468,000

1,7400,2900,0030,0022,1670,7740,0010,0225,000

0,1311,8392,000

0,0000,0070,007

15,007

2

Bk 962.7.94core

57,700,0411,460,002,385,770,0511,571,400,076,520,04

2,2099,19

7,8800,1208,000

1,7240,2440,0000,0042,3550,6590,0060,0075,000

0,2051,7261,931

0,0000,0070,007

14,938

2

Bk 972.7.94core

57,660,0511,660,142,126,000,0611,401,300,156,700,02

2,2099,46

7,8640,1368,000

1,7380,2170,0150,0052,3170,6850,0070,0155,000

0,1901,7721,962

0,0000,0040,004

14,965

2

Bk 9102.7.94core

56,250,0510,820,022,316,710,0511,883,040,125,830,07

2,1799,33

7,7590,2418,000

1,5180,2400,0020,0052,4430,7740,0060,0125,000

0,4491,5512,000

0,0080,0130,021

15,021

2

Bk 9112.7.94core

57,350,0111,730,023,604,640,0011,851,140,066,780,05

2,2099,43

7,8070,1938,000

1,6890,3680,0020,0012,4040,5290,0000,0065,000

0,1661,7901,956

0,0000,0090,009

14,965

2

Bk 9423.2.94rim

57,780,0211,800,052,365,230,0211,481,060,176,570,04

2,1998,77

7,8950,1058,000

1,7950,2430,0050,0022,3380,5970,0020,0175,000

0,1551,7411,896

0,0000,0070,007

14,903

2

Bk 9123.2.94arim

58,200,0212,010,032,325,180,0511,551,040,166,620,03

2,2199,42

7,8940,1068,000

1,8130,2370,0030,0022,3350,5870,0060,0165,000

0,1511,7411,892

0,0000,0050,005

14,897

2

Bk 9223.2.94arim

58,010,0711,560,032,485,220,0111,591,090,176,540,03

2,2099,00

7,9090,0918,000

1,7670,2540,0030,0072,3550,5950,0010,0175,000

0,1591,7291,888

0,0000,0050,005

14,893

2

C-28 Appendix C Table C5/C6 glaucophane/clinozoisite

position means analysis of: i(x), inclusion of czo in mineral x, core is core position in a czox grain, mineral x, rimposition in czo grain in contact with mineral x, mineral x(i), czo at an inclusion of mineral x in czo



H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH


Bk 9323.2.94arim

55,970,0311,200,025,463,890,0611,791,970,205,850,21

2,1898,84

7,7120,2888,000

1,5310,5660,0020,0032,4210,4490,0070,0205,000

0,2911,5631,854

0,0000,0380,038

14,891

2

Bk 9423.2.94arim

57,060,0211,350,012,735,560,0111,821,880,176,360,06

2,1999,22

7,8150,1858,000

1,6470,2820,0010,0022,4130,6370,0010,0175,000

0,2761,6891,965

0,0000,0110,011

14,975

2

Cig 91-17017.6.93rim

58,270,0111,650,001,396,940,0511,160,920,087,080,03

2,2099,78

7,9250,0758,000

1,7920,1420,0000,0012,2620,7900,0060,0085,000

0,1341,8662,000

0,0010,0050,006

15,006

2

Cig 91-17117.6.93rim

57,870,0111,660,001,278,100,0010,510,880,057,150,03

2,1999,73

7,9140,0868,000

1,7940,1310,0000,0012,1420,9270,0000,0055,000

0,1291,8712,000

0,0250,0050,030

15,030

2

Cig 91-17217.6.93core

58,470,0111,750,021,127,540,0410,790,640,077,270,03

2,2199,96

7,9460,0548,000

1,8280,1150,0020,0012,1860,8570,0050,0075,000

0,0931,9072,000

0,0090,0050,014

15,014

2

Cig 91-17917.6.93rim

57,400,0711,740,021,388,580,0010,201,050,057,060,04

2,1999,77

7,8760,1248,000

1,7750,1430,0020,0052,0860,9840,0000,0055,000

0,1541,8462,000

0,0330,0070,040

15,040

2

Cig 91-18117.6.93rim

58,350,0211,810,021,426,580,0311,310,770,017,160,05

2,2199,74

7,9210,0798,000

1,8110,1450,0020,0012,2890,7470,0030,0015,000

0,1121,8852,000

0,0000,0090,009

15,009

2

Cig 91-18817.6.93rim

58,860,1811,570,011,326,460,0211,590,640,017,320,02

2,22100,21

7,9470,0538,000

1,7880,1340,0010,0132,3320,7290,0020,0015,000

0,0931,9072,000

0,0090,0040,012

15,012

2

position means analysis of: core is core position in a gln grain, rim is rim position in a gln grain


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe

Bk 10B2618.10.93sympl

38,6025,5210,9723,44

1,9198,53

3,026

2,3580,6473,005

1,969

1,000

0,644

Bk 10B2718.10.93core

39,1929,135,9824,07

1,9598,37

3,020

2,6460,3472,992

1,987

1,000

0,349

Bk 10B2818.10.93core

39,1529,215,7924,03

1,9498,18

3,021

2,6560,3362,993

1,987

1,000

0,339

Bk 10B1119.10.93asympl

37,8026,219,2523,03

1,8896,29

3,014

2,4630,5553,018

1,968

1,000

0,545


37,9128,465,6823,34

1,8995,39

3,011

2,6640,3393,003

1,986

1,000

0,338

Bk 10B1319.10.93acore

38,0828,096,6923,94

1,9196,80

2,990

2,6000,3952,995

2,014

1,000

0,397


37,6326,049,7423,72

1,8997,13

2,979

2,4290,5803,009

2,012

1,000

0,575

Bk 10B1519.10.93aclz

38,3429,485,4724,34

1,9497,63

2,970

2,6910,3193,010

2,020

1,000

0,316


38,0626,818,3523,69

1,9096,91

3,005

2,4950,4962,991

2,004

1,000

0,501

Bk 10B2119.10.93acore

38,2727,627,7123,95

1,9297,55

2,993

2,5460,4543,000

2,007

1,000

0,454

Bk 10B2219.10.93aclz

38,4028,177,0024,28

1,9397,85

2,986

2,5820,4102,991

2,023

1,000

0,413

normed on 8 kations, all iron assumed to be Fe3

C-29Appendix C Table C6 clinozoisite

position means analysis of: i(x), inclusion of czo in mineral x, core is core position in a czo grain, mineral x, rimposition in czo grain in contact with mineral x, mineral x(i), czo at an inclusion of mineral x in czo


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


Bk 171225.7.94sympl

38,1926,189,7123,53

1,9097,61

3,008

2,4300,5763,006

1,986

1,000

0,572

Bk 171325.7.94core

37,9427,307,8923,79

1,9096,92

2,989

2,5350,4683,003

2,008

1,000

0,467

Bk 18225.8.94amph

37,9227,188,7623,75

1,9197,61

2,974

2,5130,5173,030

1,996

1,000

0,502

Bk 18235.8.94core

38,2227,228,4623,77

1,9197,67

2,994

2,5130,4993,011

1,995

1,000

0,493

Bk 18245.8.94par

38,1427,088,6023,76

1,9197,58

2,992

2,5040,5083,011

1,997

1,000

0,502

Bk 18106.8.94rut

38,7127,698,3623,59

1,9398,35

3,009

2,5370,4893,026

1,965

1,000

0,477

Bk 39213.3.93clz

37,5226,209,2124,18

1,9097,11

2,965

2,4400,5482,988

2,047

1,000

0,555

Bk 39313.3.93sympl

37,9627,018,1724,00

1,9097,14

2,987

2,5050,4842,989

2,024

1,000

0,489

Bk 39413.3.93core

37,8726,898,4123,59

1,9096,76

2,995

2,5060,5013,007

1,999

1,000

0,49

Bk 39513.3.93clz

37,9426,558,8623,83

1,9097,18

2,992

2,4680,5262,994

2,014

1,000

0,529

Bk 39613.3.93clz

37,9826,429,0123,73

1,9097,14

2,999

2,4580,5352,994

2,007

1,000

0,539

Bk 39713.3.93clz

38,0927,268,4523,62

1,9197,42

2,991

2,5230,4993,022

1,987

1,000

0,488

Bk 39813.3.93clz

37,8328,895,7623,26

1,9095,74

2,993

2,6930,3433,036

1,971

1,000

0,331

Bk 10B2319.10.93acore

38,4428,925,4123,32

1,9096,09

3,027

2,6840,3213,005

1,968

1,000

0,319

Bk 10B2419.10.93aamph

38,8025,6211,1723,05

1,9198,64

3,040

2,3660,6593,025

1,935

1,000

0,643

Bk 10B2519.10.93aamph

38,2627,487,8024,09

1,9297,63

2,991

2,5320,4592,991

2,018

1,000

0,463

Bk 10B2619.10.93acore

38,5429,125,6223,99

1,9397,27

2,999

2,6710,3293,000

2,000

1,000

0,329

Bk 10B2719.10.93acore

38,2827,657,4824,11

1,9297,52

2,993

2,5480,4402,988

2,020

1,000

0,445

Bk 10B2819.10.93aclz

38,3428,865,4923,86

1,9196,55

3,006

2,6660,3242,990

2,004

1,000

0,327


38,4828,295,7624,15

1,9196,68

3,017

2,6140,3402,954

2,029

1,000

0,356

Bk 17925.7.94ab

37,7725,8310,2823,47

1,8997,35

2,989

2,4090,6123,021

1,990

1,000

0,599

Bk 171025.7.94clz

38,2727,598,0523,78

1,9297,69

2,992

2,5420,4733,016

1,992

1,000

0,466

Bk 171125.7.94core

38,1026,1810,0423,49

1,9197,81

2,998

2,4280,5943,022

1,980

1,000

0,581

Bk 17259.7.94clz

38,0925,6510,5523,69

1,9097,98

2,998

2,3790,6253,004

1,998

1,000

0,622

Bk 17269.7.94ab

37,5724,8411,3623,46

1,8897,23

2,990

2,3300,6803,010

2,000

1,000

0,673

Bk 17279.7.94sympl

37,7825,3610,9123,55

1,8997,60

2,989

2,3650,6503,015

1,996

1,000

0,640

Bk 17389.7.94ab

37,8925,4710,9523,33

1,9097,64

2,997

2,3740,6523,026

1,977

1,000

0,635

Bk 17399.7.94clz

38,8926,7510,0624,20

1,9599,90

2,994

2,4270,5833,010

1,996

1,000

0,577

Bk 17409.7.94sympl

38,4725,2511,4523,68

1,9298,85

3,011

2,3290,6743,003

1,986

1,000

0,672

Bk 17469.7.94core

38,1627,008,5723,79

1,9197,52

2,995

2,4980,5063,004

2,001

1,000

0,504

Bk 186125.7.94sympl

38,1629,355,3223,88

1,9296,71

2,983

2,7040,3133,017

2,000

1,000

0,308

Bk 186225.7.94core

37,9928,975,8723,64

1,9196,47

2,983

2,6810,3473,028

1,989

1,000

0,337

Bk 18195.8.94core

38,1727,508,1123,95

1,9297,73

2,984

2,5330,4773,011

2,006

1,000

0,472

C-30 Appendix C Table C6 clinozoisite



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


Bk 39913.3.93clz

38,3630,244,6924,05

1,9497,34

2,971

2,7600,2733,034

1,996

1,000

0,264

Bk 391013.3.93clz

37,9228,486,2923,73

1,9096,42

2,985

2,6420,3733,014

2,001

1,000

0,367

Bk 391213.3.93sympl

37,8227,158,2423,76

1,9096,97

2,982

2,5230,4893,011

2,007

1,000

0,483

Bk 391313.3.93core

38,2428,406,5123,63

1,9196,78

3,001

2,6270,3853,012

1,987

1,000

0,380

Bk 391513.3.93clz

37,8426,978,7623,64

1,9097,21

2,981

2,5040,5193,023

1,995

1,000

0,507

Bk 391613.3.93clz

38,2227,218,4224,04

1,9297,89

2,986

2,5060,4953,001

2,013

1,000

0,495

Bk 391713.3.93par

37,9127,557,7023,71

1,9096,87

2,986

2,5570,4563,014

2,001

1,000

0,450

Bk 391813.3.93par

38,0827,637,7923,93

1,9197,43

2,982

2,5500,4593,010

2,008

1,000

0,455

Bk 391913.3.93par

37,9427,358,4123,99

1,9297,69

2,970

2,5230,4963,019

2,012

1,000

0,486

Bk 392013.3.93par

37,9227,198,2723,74

1,9097,12

2,985

2,5230,4903,013

2,002

1,000

0,484

Bk 392113.3.93clz

38,2429,135,6823,81

1,9296,86

2,989

2,6830,3343,017

1,994

1,000

0,328

Bk 392213.3.93clz

38,2129,006,0323,95

1,9297,19

2,980

2,6650,3543,019

2,001

1,000

0,347

Bk 392313.3.93sympl

38,2828,157,6123,63

1,9297,67

2,988

2,5890,4473,036

1,976

1,000

0,431

Bk 392413.3.93sympl

38,0327,168,7623,47

1,9197,42

2,989

2,5160,5183,034

1,977

1,000

0,501

Bk 39924.6.92i (grt)

37,3128,946,3623,29

1,9095,90

2,951

2,6970,3783,076

1,973

1,000

0,352

Bk 391724.6.92i (grt)

37,9628,427,3323,49

1,9197,20

2,973

2,6230,4323,056

1,971

1,000

0,409

Bk 392024.6.92par

37,2526,479,1023,66

1,8996,48

2,961

2,4800,5443,024

2,015

1,000

0,532

Bk 392124.6.92clz

37,2827,777,4023,51

1,8995,96

2,960

2,5980,4423,041

2,000

1,000

0,425

Bk 392224.6.92core

37,5126,578,6823,90

1,8996,66

2,972

2,4810,5182,999

2,029

1,000

0,518

Bk 393524.6.92par

37,7527,427,4823,82

1,9096,47

2,984

2,5540,4452,999

2,017

1,000

0,445

Bk 393624.6.92clz

38,0228,835,7323,75

1,9196,33

2,989

2,6710,3393,011

2,000

1,000

0,336

Bk 394224.6.92sympl

37,1725,869,4823,77

1,8896,28

2,966

2,4320,5693,001

2,032

1,000

0,568

Bk 394424.6.92core

37,9129,395,4623,97

1,9296,73

2,964

2,7080,3213,029

2,008

1,000

0,312

Bk 394524.6.92cpx

37,5226,768,8123,75

1,9096,84

2,968

2,4950,5253,019

2,013

1,000

0,515

Bk 394624.6.92core

37,5626,878,6223,47

1,8996,52

2,979

2,5120,5153,026

1,994

1,000

0,501

Bk 394724.6.92clz

37,6427,916,9123,74

1,9096,20

2,976

2,6010,4113,012

2,011

1,000

0,406

Bk 394824.6.92par

37,5026,908,3923,57

1,8996,36

2,977

2,5170,5013,018

2,005

1,000

0,492

Bk 39128.1.93i (grt)

37,4327,407,8623,12

1,8895,81

2,982

2,5730,4713,044

1,974

1,000

0,451

Bk 39228.1.93i (grt)

38,3629,854,6323,46

1,9196,30

3,004

2,7550,2733,028

1,968

1,000

0,266

Bk 391728.8.92cpx

37,9228,736,8923,92

1,9297,46

2,957

2,6400,4043,045

1,998

1,000

0,387

Bk 391928.8.92cpx

37,6828,557,2224,21

1,9297,66

2,935

2,6210,4233,044

2,021

1,000

0,405

Bk 395,25.5.92cpx

37,7528,605,6923,90

1,9095,94

2,980

2,6610,3382,999

2,021

1,000

0,338

Bk 396,25.5.92core

37,6426,348,7523,79

1,8996,52

2,989

2,4650,5232,987

2,024

1,000

0,529


C-31Appendix C Table C6 clinozoisite



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


Bk 397,25.5.92sympl

37,6126,138,4823,94

1,8896,16

2,996

2,4530,5082,961

2,043

1,000

0,529

Bk 4549.7.94vein

38,3728,526,3323,87

1,9297,09

3,000

2,6280,3733,001

2,000

1,000

0,372

Bk 4559.7.94vein

38,5028,256,8124,10

1,9397,66

2,998

2,5920,3992,992

2,011

1,000

0,403

Bk 4569.7.94vein

38,4528,047,4523,83

1,9297,77

2,997

2,5760,4373,013

1,990

1,000

0,431

Bk 4589.7.94vein

38,5327,896,9924,01

1,9297,42

3,011

2,5680,4112,979

2,010

1,000

0,420

Bk 4599.7.94vein

38,8528,756,5023,80

1,9397,90

3,014

2,6290,3803,008

1,978

1,000

0,376

Bk 4609.7.94vein

38,3328,356,4823,62

1,9196,78

3,008

2,6230,3833,005

1,986

1,000

0,381

Bk 4619.7.94vein

38,1528,425,9323,76

1,9096,26

3,005

2,6380,3522,990

2,005

1,000

0,355

Bk 4629.7.94vein

38,4028,586,3523,65

1,9296,98

3,006

2,6370,3743,011

1,984

1,000

0,370

Bk 4639.7.94vein

38,5227,936,9823,85

1,9297,28

3,014

2,5760,4112,987

1,999

1,000

0,417

Bk 76726.4.93i (grt)

38,0228,516,9323,52

1,9196,98

2,981

2,6340,4093,044

1,976

1,000

0,392

Bk 76826.4.93i (grt)

37,9227,717,4523,23

1,8996,31

3,001

2,5850,4443,029

1,970

1,000

0,431

Bk 76926.4.93i (grt)

37,6027,388,2023,51

1,9096,69

2,971

2,5500,4883,038

1,991

1,000

0,470

Bk 77026.4.93i (grt)

37,6427,098,7623,35

1,9096,84

2,976

2,5250,5213,046

1,978

1,000

0,498

Bk 7927.8.92amph

37,6028,156,8123,99

1,9096,55

2,960

2,6120,4043,016

2,024

1,000

0,397

Bk 71027.8.92ap

37,7127,846,9923,47

1,8996,01

2,989

2,6010,4173,018

1,993

1,000

0,410

Bk 71127.8.92cpx

37,3727,927,1223,52

1,8995,93

2,965

2,6110,4253,036

1,999

1,000

0,411

Bk 71227.8.92core

37,4628,336,4823,81

1,9096,08

2,960

2,6390,3853,024

2,016

1,000

0,376

Bk 71327.8.92cpx

37,8328,656,0624,37

1,9296,91

2,959

2,6410,3572,998

2,043

1,000

0,357

Bk 71427.8.92par

37,5927,657,2823,59

1,8996,11

2,979

2,5830,4343,017

2,003

1,000

0,427

Bk 72027.8.92par

37,4728,226,6723,64

1,8996,00

2,966

2,6320,3973,030

2,005

1,000

0,386

Bk 72127.8.92par

37,6527,507,9124,07

1,9197,13

2,959

2,5470,4683,015

2,027

1,000

0,461

Bk 72227.8.92cpx

37,5028,127,1323,82

1,9096,57

2,955

2,6110,4233,034

2,011

1,000

0,409

Bk 7147.7.92ab

37,2827,567,3623,97

1,8996,17

2,953

2,5730,4393,012

2,035

1,000

0,433

Bk 7157.7.92ab

37,4627,317,9223,65

1,8996,34

2,969

2,5510,4733,023

2,008

1,000

0,462

Bk 7167.7.92clz

37,5127,826,9923,91

1,9096,23

2,966

2,5930,4163,008

2,026

1,000

0,412

Bk 7177.7.92par

37,0028,636,3223,56

1,8995,51

2,938

2,6790,3783,057

2,005

1,000

0,357

Bk 7527.7.92par

37,2326,797,9823,70

1,8895,70

2,972

2,5210,4793,000

2,027

1,000

0,479

Bk 7537.7.92par

37,3827,198,1123,82

1,8996,50

2,959

2,5370,4833,020

2,020

1,000

0,474

Bk 7547.7.92gnt

37,6627,337,8223,91

1,9096,72

2,972

2,5420,4653,006

2,022

1,000

0,462

Bk 8214.3.93core

38,4228,576,1623,71

1,9196,86

3,010

2,6380,3633,001

1,990

1,000

0,363

Bk 8314.3.93par

37,8727,987,0123,78

1,9096,64

2,982

2,5970,4163,012

2,006

1,000

0,411

Bk 8414.3.93core

38,1328,496,7123,23

1,9096,56

3,001

2,6430,3983,040

1,959

1,000

0,382


C-32 Appendix C Table C6 clinozoisite


Bk 8514.3.93clz

37,6727,487,4823,63

1,8996,26

2,984

2,5650,4463,011

2,005

1,000

0,441


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


Bk 8814.3.93clz

38,1027,657,7923,69

1,9197,23

2,990

2,5580,4603,018

1,992

1,000

0,452

Bk 8914.3.93par

37,8328,266,5623,55

1,9096,20

2,987

2,6300,3903,020

1,993

1,000

0,382

Bk 81014.3.93clz

38,0428,027,0523,65

1,9196,76

2,992

2,5980,4173,015

1,993

1,000

0,411

Bk 81114.3.93sympl

37,7527,077,8623,49

1,8996,17

2,998

2,5340,4703,003

1,999

1,000

0,468

Bk 82114.3.93par

38,1229,385,1523,81

1,9196,46

2,986

2,7120,3033,016

1,998

1,000

0,299

Bk 82214.3.93zoi

38,2529,414,9324,10

1,9296,69

2,987

2,7070,2902,997

2,016

1,000

0,291

Bk 912.7.94par

38,1427,607,3123,92

1,9196,97

2,997

2,5560,4322,989

2,014

1,000

0,437

Bk 922.7.94core

38,5029,255,1524,17

1,9397,07

2,998

2,6840,3012,986

2,016

1,000

0,306

Bk 932.7.94par

38,1627,667,3623,70

1,9196,88

3,002

2,5650,4363,000

1,998

1,000

0,435

Bk 9282.7.94zoi

38,1528,166,8323,72

1,9196,86

2,995

2,6060,4043,009

1,995

1,000

0,400

Bk 9292.7.94par

38,3226,668,9223,58

1,9197,48

3,014

2,4710,5282,999

1,987

1,000

0,529

Bk 9302.7.94clz

38,6729,675,2223,99

1,9497,55

2,996

2,7090,3043,013

1,991

1,000

0,300

Bk 9312.7.94sympl

37,6725,5710,3123,67

1,8997,22

2,986

2,3890,6153,004

2,010

1,000

0,613

Bk 91623.2.94par

38,0427,568,5823,72

1,9297,90

2,972

2,5380,5043,042

1,986

1,000

0,484

Bk 91723.2.94core

37,9627,598,9623,56

1,9298,06

2,964

2,5390,5263,065

1,971

1,000

0,494

Bk 91823.2.94core

38,3929,935,8223,90

1,9498,04

2,963

2,7230,3383,061

1,976

1,000

0,319

Bk 91923.2.94amph

38,4829,166,4623,96

1,9498,05

2,978

2,6600,3763,036

1,987

1,000

0,363

Bk 92123.2.94amph

38,2229,077,0923,99

1,9498,37

2,954

2,6480,4123,060

1,986

1,000

0,389

Bk 92223.2.94ab

38,2228,917,4323,78

1,9498,35

2,958

2,6370,4333,070

1,972

1,000

0,405

Bk 92323.2.94par

37,9627,298,5923,80

1,9197,64

2,974

2,5210,5073,027

1,998

1,000

0,493

Bk 92423.2.94par

38,1228,756,8123,85

1,9297,54

2,970

2,6400,3993,039

1,991

1,000

0,384

Bk 92523.2.94par

38,3228,457,3123,90

1,9397,98

2,977

2,6050,4283,033

1,990

1,000

0,414

Bk 92623.2.94core

38,0728,507,4023,98

1,9397,96

2,959

2,6110,4333,044

1,997

1,000

0,415

Bk 92823.2.94clz

38,3329,016,6324,11

1,9498,08

2,967

2,6470,3863,033

2,000

1,000

0,374

Bk 92923.2.94core

38,5830,325,3324,24

1,9598,48

2,959

2,7410,3083,049

1,992

1,000

0,294

Bk 93023.2.94par

37,7327,997,6023,75

1,9197,07

2,963

2,5900,4493,039

1,998

1,000

0,432

Bk 93323.2.94par

38,2829,196,3224,16

1,9497,95

2,964

2,6640,3683,032

2,004

1,000

0,357

Bk 93523.2.94clz

38,3828,457,3123,54

1,9297,68

2,991

2,6140,4293,043

1,966

1,000

0,411

Bk 93623.2.94par

38,3428,817,0024,03

1,9498,18

2,969

2,6290,4083,037

1,994

1,000

0,393

Bk 93723.2.94par

38,3829,296,4923,94

1,9498,10

2,968

2,6700,3783,048

1,984

1,000

0,361

Bk 93823.2.94par

38,2128,097,6323,97

1,9397,91

2,975

2,5780,4473,025

2,000

1,000

0,436

Bk 93923.2.94core

38,4329,496,4724,18

1,9598,56

2,957

2,6750,3753,049

1,994

1,000

0,357

C-33Appendix C Table C6/C7 clinozoisite/zoisite

position means analysis of: i(x), inclusion of czo/zoi in mineral x, core is core position in a czo/zoi grain, mineral x,rim position in czo/zoi grain in contact with mineral x, mineral x(i), czo/zoi at an inclusion of mineral x in czo/zoi


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe



SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe


Bk 954.3.94zoi

39,2329,346,6324,23

1,9699,43

2,996

2,6410,3813,022

1,982

1,000

0,373

Bk 964.3.94chl

39,1829,566,4024,06

1,9699,20

2,996

2,6640,3683,033

1,971

1,000

0,357

Bk 974.3.94chl

38,9228,747,2723,98

1,9598,91

2,995

2,6070,4213,028

1,977

1,000

0,410

Bk 984.3.94core

38,8529,256,6524,00

1,9598,75

2,987

2,6510,3853,035

1,977

1,000

0,371

Cig 91-11316.6.93i (grt)

38,0626,639,3522,83

1,8996,87

3,016

2,4870,5573,045

1,939

1,000

0,533

Cig 91-15517.6.93i (grt)

38,4328,576,8724,14

1,9398,01

2,981

2,6120,4013,013

2,006

1,000

0,396

Cig 91-15617.6.93i (grt)

38,4928,487,0224,08

1,9398,07

2,985

2,6030,4103,013

2,001

1,000

0,405

Bk 9824.2.94chl

38,2129,605,9324,02

1,9497,77

2,959

2,7020,3463,048

1,993

1,000

0,330

Bk 9924.2.94chl

38,3029,426,0124,21

1,9497,94

2,962

2,6820,3503,032

2,006

1,000

0,339

Bk 91024.2.94chl

38,0928,867,0623,98

1,9397,99

2,956

2,6390,4123,051

1,993

1,000

0,392

Bk 91124.2.94chl

38,0328,457,4823,09

1,9197,05

2,985

2,6320,4423,073

1,942

1,000

0,412

Bk 91224.2.94chl

38,3229,586,0323,90

1,9497,83

2,967

2,6990,3523,051

1,983

1,000

0,335

Bk 91324.2.94chl

37,3725,4910,9723,57

1,8997,40

2,962

2,3820,6543,036

2,002

1,000

0,632

Bk 96924.2.94chl

38,2230,005,2524,26

1,9497,73

2,954

2,7320,3053,038

2,009

1,000

0,294

Bk 97424.2.94sympl

37,8526,729,3123,89

1,9197,77

2,970

2,4710,5503,021

2,009

1,000

0,539

Bk 97524.2.94core

38,2028,347,2923,81

1,9297,64

2,979

2,6040,4283,032

1,989

1,000

0,414

Bk 97624.2.94zoi

38,0729,246,1623,95

1,9397,42

2,962

2,6810,3603,042

1,996

1,000

0,346

Bk 944.3.94zoi

39,2729,316,6024,28

1,9699,46

2,998

2,6370,3793,016

1,986

1,000

0,373

Bk 8114.3.93par(i)

39,0531,861,7124,34

1,9596,96

3,005

2,8890,0992,988

2,007

1

0,10

Bk 8714.3.93core

38,3531,142,3424,95

1,9496,78

2,963

2,8350,1362,972

2,065

1

0,14

Bk 9272.7.94par

39,4631,532,5424,74

1,9798,27

3,005

2,8300,1462,976

2,019

1

0,15

Bk 91423.2.94par

39,4132,792,2624,14

1,9898,59

2,985

2,9270,1293,056

1,959

1

0,12

Bk 91523.2.94core

38,7431,943,0624,65

1,9798,39

2,949

2,8660,1753,041

2,010

1

0,17

Bk 92723.2.94core

39,3032,812,0124,41

1,9898,53

2,976

2,9280,1153,043

1,981

1

0,11

Bk 93123.2.94core

38,7732,331,8224,04

1,9596,96

2,982

2,9310,1053,036

1,981

1

0,10

Bk 93223.2.94par(i)

39,0232,891,6224,58

1,9798,12

2,964

2,9440,0933,036

2,000

1

0,09

Bk 9124.2.94qtz(i)

38,9732,482,1124,39

1,9797,95

2,970

2,9180,1213,039

1,992

1

0,12

Bk 97024.2.94core

38,7832,252,5124,63

1,9798,17

2,953

2,8940,1443,038

2,009

1

0,14

Bk 97124.2.94qtz(i)

39,2933,101,8024,45

1,9898,64

2,969

2,9480,1023,051

1,980

1

0,10

C-34 Appendix C Table C7/C8 zoisite/paragonite

position means analysis of: i(x), inclusion of zoi in mineral x, core is core position in a zoi grain, mineral x, rimposition in zoi grain in contact with mineral x, mineral x(i), zoi at an inclusion of mineral x in zoi


sampleanalysisdate

SiO2Al2O3Fe2O3MgOCaONa2OK2Ototal

H2O

Si

AloFe3

MgCa

NaK

sum

OH

Bk 10B2119.10.93

47,1237,841,070,670,136,841,4295,09

4,66

3,030

2,8680,0522,920

0,0640,0090,073

0,8530,1190,972

4,141

2

Bk 18156.8.94

47,3239,800,460,180,217,010,8395,81

4,73

3,003

2,9770,0222,998

0,0170,0140,031

0,8620,0690,931

4,036

2

Bk 18166.8.94

47,3738,760,570,250,176,671,3195,10

4,68

3,033

2,9250,0272,953

0,0240,0120,036

0,8280,1090,937

4,016

2

Bk 18176.8.94

46,5739,470,420,150,207,130,6794,61

4,67

2,993

2,9890,0203,010

0,0140,0140,028

0,8880,0560,944

4,051

2

Bk 391,213.3.93

46,3939,830,300,140,157,590,2794,67

4,67

2,977

3,0120,0143,027

0,0130,0100,024

0,9440,0230,967

4,070

2

Bk 392,213.3.93

46,9239,940,490,170,257,380,2895,43

4,71

2,986

2,9950,0233,019

0,0160,0170,033

0,9110,0230,934

4,066

2

Bk 394113.3.93

46,3538,970,480,220,157,680,5094,35

4,64

2,992

2,9650,0232,988

0,0210,0100,032

0,9610,0421,003

4,101

2

Bk 394213.3.93

46,2739,420,540,320,187,490,4094,62

4,66

2,976

2,9880,0263,014

0,0310,0120,043

0,9340,0340,968

4,121

2

Bk 394313.3.93

47,3239,080,420,470,317,580,2895,46

4,71

3,013

2,9330,0202,953

0,0450,0210,066

0,9360,0230,959

4,084

2

Bk 394513.3.93

46,9438,630,420,420,177,590,4494,61

4,66

3,018

2,9270,0202,947

0,0400,0120,052

0,9460,0370,983

4,075

2

Bk 394713.3.93

47,1637,680,480,240,197,670,4193,83

4,63

3,056

2,8780,0232,901

0,0230,0130,036

0,9640,0350,998

4,019

2

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH

Cig 90/40111.6.91bclz

39,1431,472,9024,02

1,9597,53

3,006

2,8490,1683,017

1,977

1

0,16


SiO2Al2O3Fe2O3CaO

H2OTotal

Si

AlFe3

Ca

OH

XAl2Fe

Bk 97224.2.94core

39,0632,931,9624,55

1,9898,50

2,958

2,9390,1113,050

1,992

1

0,11

Bk 97324.2.94core

38,9432,472,5824,43

1,9798,41

2,958

2,9070,1473,054

1,988

1

0,14

Bk 914.3.94clz

40,0832,732,4824,92

2,01100,21

2,990

2,8780,1393,017

1,992

1

0,14

Bk 924.3.94clz

39,8732,212,8524,70

1,9999,63

2,997

2,8530,1613,014

1,989

1

0,16

Cig 90/40101.6.91bcore

38,8931,442,1024,62

1,9597,05

2,994

2,8530,1222,975

2,031

1

0,12

Bk 394813.3.93

46,6240,010,360,130,187,080,3394,71

4,68

2,984

3,0190,0173,036

0,0120,0120,025

0,8790,0280,906

4,026

2

Bk 394913.3.93

46,4539,850,360,200,177,400,3594,78

4,68

2,977

3,0100,0173,027

0,0190,0120,031

0,9200,0290,949

4,072

2

Bk 395013.3.93

47,1139,660,470,140,206,960,5795,11

4,70

3,006

2,9820,0223,005

0,0130,0140,027

0,8610,0470,908

4,012

2

Bk 395113.3.93

46,4340,000,440,130,257,030,3394,61

4,68

2,977

3,0230,0213,044

0,0120,0170,030

0,8740,0280,901

4,048

2

Bk 395213.3.93

46,7539,330,380,220,237,380,5594,84

4,68

2,998

2,9720,0182,991

0,0210,0160,037

0,9180,0460,964

4,064

2

Bk 395313.3.93

46,8539,500,330,250,187,410,7495,26

4,69

2,994

2,9750,0162,991

0,0240,0120,036

0,9180,0620,980

4,075

2

Bk 395413.3.93

46,6639,900,320,140,237,080,5594,88

4,69

2,986

3,0090,0163,025

0,0130,0160,029

0,8780,0460,924

4,038

2

Bk 395513.3.93

46,6139,490,410,220,567,360,5995,24

4,69

2,982

2,9770,0202,997

0,0210,0380,059

0,9130,0490,962

4,118

2

Bk 395613.3.93

46,8039,150,400,270,217,200,7194,74

4,67

3,005

2,9620,0192,982

0,0260,0140,040

0,8960,0590,956

4,057

2

Bk 395713.3.93

46,9339,470,320,280,186,970,9095,05

4,69

3,002

2,9760,0162,991

0,0270,0120,039

0,8640,0750,940

4,040

2

Bk 395813.3.93

46,8039,600,340,220,207,400,6595,21

4,69

2,991

2,9820,0172,999

0,0210,0140,035

0,9170,0540,971

4,072

2

normed on 22 oxygen, all iron assumed to be Fe3


C-35Appendix C Table C8 paragonite

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH

Bk 391024.6.92

46,8937,071,300,830,096,851,2294,25

4,62

3,042

2,8340,0632,898

0,0800,0060,087

0,8620,1030,965

4,163

2

Bk 392324.6.92

46,0839,360,360,250,197,440,4094,08

4,64

2,978

2,9980,0173,016

0,0240,0130,037

0,9320,0340,966

4,091

2

Bk 392424.6.92

46,2339,430,330,260,176,690,8393,94

4,64

2,989

3,0050,0163,021

0,0250,0120,037

0,8390,0700,909

4,035

2

Bk 392524.6.92

46,0939,530,320,150,227,260,3993,96

4,64

2,979

3,0110,0163,027

0,0140,0150,030

0,9100,0330,943

4,061

2

Bk 393024.6.92

45,8239,770,300,080,217,210,3093,69

4,63

2,968

3,0360,0153,051

0,0080,0150,022

0,9060,0250,931

4,056

2

Bk 393124.6.92

45,8439,800,260,120,196,800,3293,33

4,62

2,975

3,0440,0123,056

0,0120,0130,025

0,8560,0270,883

4,014

2

Bk 393224.6.92

45,5439,290,320,150,187,440,5393,45

4,60

2,966

3,0160,0163,032

0,0150,0130,027

0,9400,0450,985

4,102

2

Bk 393324.6.92

45,8239,220,460,150,167,300,5993,70

4,62

2,976

3,0030,0223,025

0,0150,0110,026

0,9190,0500,969

4,090

2

Bk 394924.6.92

46,0339,350,320,220,177,220,6393,94

4,63

2,980

3,0020,0163,018

0,0210,0120,033

0,9060,0530,959

4,075

2

Bk 395024.6.92

46,2239,530,380,190,177,310,5894,38

4,65

2,979

3,0030,0183,021

0,0180,0120,030

0,9130,0490,962

4,080

2

Bk 395124.6.92

46,0039,070,470,240,137,070,8693,84

4,62

2,985

2,9880,0233,011

0,0230,0090,032

0,8900,0730,962

4,083

2

Bk 393528.1.93

47,2538,560,910,400,137,500,2695,01

4,68

3,024

2,9090,0442,952

0,0380,0090,047

0,9310,0220,952

4,087

2

Bk 393628.1.93

47,3838,100,900,610,107,460,1794,72

4,67

3,039

2,8800,0432,924

0,0580,0070,065

0,9280,0140,942

4,083

2

Bk 393828.1.93

46,5139,210,720,120,157,390,1894,28

4,66

2,996

2,9770,0353,012

0,0120,0100,022

0,9230,0150,938

4,063

2

Bk 393928.1.93

46,7038,580,710,400,137,320,2194,05

4,64

3,015

2,9360,0352,970

0,0380,0090,047

0,9160,0180,934

4,068

2

Bk 394028.1.93

47,4838,260,760,210,127,360,9495,13

4,68

3,043

2,8900,0362,926

0,0200,0080,028

0,9150,0790,993

4,049

2

Bk 394128.1.93

45,7439,330,690,180,127,430,9394,42

4,63

2,960

2,9990,0343,033

0,0170,0080,026

0,9320,0781,011

4,162

2

Bk 394228.1.93

45,9439,290,460,110,157,030,4993,47

4,62

2,985

3,0080,0223,031

0,0110,0100,021

0,8860,0410,927

4,045

2

Bk 394328.1.93

46,3838,730,580,340,297,390,1693,87

4,63

3,002

2,9540,0282,982

0,0330,0200,053

0,9270,0130,941

4,085

2

Bk 394428.1.93

46,3739,700,780,090,567,470,4195,38

4,69

2,965

2,9920,0373,029

0,0090,0380,047

0,9260,0340,960

4,158

2

Bk 394628.1.93

46,9538,250,910,240,497,440,1094,38

4,65

3,025

2,9050,0442,949

0,0230,0340,057

0,9300,0080,938

4,089

2

Bk 394728.1.93

46,6339,070,670,130,137,400,6094,63

4,66

3,000

2,9620,0322,995

0,0120,0090,021

0,9230,0500,973

4,075

2

Bk 394828.1.93

46,0039,790,530,090,197,230,3894,21

4,65

2,967

3,0250,0263,051

0,0090,0130,022

0,9040,0320,936

4,082

2

Bk 394928.1.93

45,8039,270,590,130,157,280,6093,82

4,62

2,972

3,0040,0293,033

0,0130,0100,023

0,9160,0510,967

4,103

2

Bk 395028.1.93

46,6939,220,920,120,257,460,4095,06

4,68

2,991

2,9610,0443,006

0,0110,0170,029

0,9270,0330,960

4,112

2

Bk 3934.5.92

46,2138,910,500,150,217,500,6494,12

4,63

2,992

2,9690,0242,993

0,0140,0150,029

0,9410,0540,995

4,096

2

Bk 395,25.5.92

46,4038,440,410,140,167,690,5393,77

4,62

3,013

2,9420,0202,962

0,0140,0110,025

0,9680,0451,013

4,064

2

Bk 397,25.5.92

45,7239,100,400,110,217,730,3893,65

4,61

2,973

2,9970,0203,016

0,0110,0150,025

0,9750,0321,007

4,113

2

Bk 39125.5.92

47,2637,720,530,120,387,720,4194,14

4,64

3,055

2,8740,0262,900

0,0120,0260,038

0,9680,0351,002

4,030

2

Bk 39135.5.92

46,4938,690,440,180,177,090,6893,74

4,62

3,014

2,9570,0222,978

0,0170,0120,029

0,8910,0570,949

4,029

2

Bk 39.12028.8.92

46,1740,080,560,060,167,650,4695,14

4,68

2,956

3,0250,0273,051

0,0060,0110,017

0,9500,0380,988

4,126

2

Bk 39.12228.8.92

46,6439,970,560,160,207,450,3995,37

4,70

2,974

3,0040,0273,031

0,0150,0140,029

0,9210,0320,954

4,095

2

Bk 39.12328.8.92

46,3040,490,310,080,277,340,3295,11

4,70

2,956

3,0470,0153,062

0,0080,0180,026

0,9090,0270,935

4,080

2




C-36 Appendix C Table C8 paragonite

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH




Bk 76027.8.92

46,3339,960,360,120,257,280,4894,78

4,68

2,971

3,0200,0173,038

0,0110,0170,029

0,9050,0400,945

4,074

2

Bk 76127.8.92

46,7039,970,420,190,146,640,8494,90

4,69

•

2,987

3,0130,0203,034

0,0180,0100,028

0,8240,0700,894

4,023

2

Bk 76227.8.92

46,6640,300,290,110,217,250,5595,37

4,71

2,973

3,0260,0143,040

0,0100,0140,025

0,8960,0460,941

4,058

2

Bk 76327.8.92

46,1839,540,410,260,196,801,1294,50

4,65

2,977

3,0040,0203,024

0,0250,0130,038

0,8500,0940,944

4,084

2

Bk 76427.8.92

46,9139,760,370,280,176,611,0395,13

4,69

2,997

2,9930,0183,011

0,0270,0120,038

0,8190,0860,904

4,027

2

Bk 76527.8.92

46,7240,010,310,170,196,920,6794,99

4,69

2,986

3,0140,0153,028

0,0160,0130,029

0,8570,0560,913

4,030

2

Bk 76627.8.92

46,3240,260,340,090,256,840,5194,61

4,68

2,970

3,0420,0173,059

0,0090,0170,026

0,8500,0430,893

4,037

2

Bk 76727.8.92

46,2940,190,420,120,156,490,6794,33

4,67

2,975

3,0440,0203,064

0,0110,0100,022

0,8090,0560,865

4,014

2

Bk 76827.8.92

46,5440,120,370,100,166,840,6094,73

4,68

2,980

3,0280,0183,046

0,0100,0110,021

0,8490,0500,899

4,022

2

Bk 76927.8.92

46,1239,770,320,110,216,750,4693,74

4,64

2,982

3,0300,0163,046

0,0110,0150,025

0,8460,0390,885

4,013

2

Bk 7707.8.92

46,4540,240,460,160,166,490,8294,78

4,68

2,974

3,0370,0223,059

0,0150,0110,026

0,8060,0680,874

4,029

2

Bk 7627.7.92

47,6640,390,910,510,236,900,2396,83

4,79

2,986

2,9820,0433,025

0,0480,0150,063

0,8380,0190,857

4,094

2

Bk 7687.7.92

47,6840,550,670,300,156,700,9697,01

4,78

2,988

2,9950,0313,026

0,0280,0100,038

0,8140,0780,892

4,058

2

Bk 82314.3.93

47,2140,890,570,130,206,460,5796,03

4,75

2,978

3,0400,0273,067

0,0120,0140,026

0,7900,0470,837

4,009

2

Bk 84614.3.93

46,5739,770,510,130,227,140,5594,89

4,68

2,983

3,0020,0253,027

0,0120,0150,028

0,8870,0460,933

4,064

2

Bk 84714.3.93

46,8139,600,440,250,186,910,8295,01

4,69

2,995

2,9860,0213,007

0,0240,0120,036

0,8570,0680,926

4,048

2

Bk 84814.3.93

47,3639,800,430,140,247,000,4395,40

4,72

3,010

2,9810,0213,002

0,0130,0160,030

0,8620,0360,898

4,000

2

Bk 84914.3.93

46,3539,170,300,120,346,440,7093,42

4,62

3,007

2,9950,0153,010

0,0120,0240,035

0,8100,0590,869

3,979

2

Bk 85014.3.93

46,7338,690,830,350,527,010,6894,81

4,66

3,004

2,9310,0402,972

0,0340,0360,069

0,8740,0570,931

4,122

2

Bk 9342.7.94

46,4439,320,480,130,257,450,3194,38

4,66

2,991

2,9840,0233,007

0,0120,0170,030

0,9300,0260,956

4,069

2

Bk 9352.7.94

46,8338,960,280,210,217,210,5894,28

4,65

3,017

2,9580,0132,971

0,0200,0140,035

0,9010,0490,949

4,017

2

Bk 94023.2.94

48,5141,660,410,160,276,540,7498,29

4,87

2,990

3,0260,0193,045

0,0150,0180,033

0,7810,0590,841

3,989

2

Bk 94123.2.94

47,8341,330,340,110,326,990,5297,44

4,82

2,977

3,0320,0163,048

0,0100,0210,032

0,8440,0420,886

4,029

2

Bk 94223.2.94

48,1441,860,440,200,566,510,9498,65

4,87

2,965

3,0380,0213,059

0,0180,0370,055

0,7770,0750,853

4,064

2

Bk 94323.2.94

47,2141,960,410,070,286,820,2797,02

4,80

2,946

3,0860,0193,106

0,0070,0190,025

0,8250,0220,847

4,042

2

Bk 94523.2.94

47,1241,360,500,110,276,860,2496,46

4,78

2,959

3,0610,0243,084

0,0100,0180,028

0,8350,0200,855

4,043

2

Bk 94623.2.94

47,3741,170,480,090,277,120,3296,82

4,79

2,967

3,0400,0233,062

0,0080,0180,027

0,8650,0260,891

4,051

2

Bk 94823.2.94

48,3341,380,530,210,236,280,9097,86

4,84

2,993

3,0200,0253,045

0,0190,0150,035

0,7540,0730,827

3,990

2

Bk 94923.2.94

47,4441,730,640,260,276,840,3497,52

4,82

2,950

3,0580,0303,088

0,0240,0180,042

0,8250,0280,852

4,085

2

Bk 95023.2.94

47,3841,330,440,080,256,980,4396,89

4,79

2,965

3,0490,0213,069

0,0070,0170,024

0,8470,0350,882

4,042

2

Bk 95123.2.94

47,8041,640,480,100,166,700,5197,39

4,82

2,972

3,0520,0223,074

0,0090,0110,020

0,8080,0410,849

4,008

2

Bk 94524.2.94

47,3840,730,340,190,247,150,3796,40

4,77

2,980

3,0200,0163,036

0,0180,0160,034

0,8720,0300,902

4,039

2

Bk 94624.2.94

47,6740,870,380,240,177,000,7397,06

4,79

2,982

3,0140,0183,031

0,0220,0110,034

0,8490,0600,909

4,043

2

C-37Appendix C Table C8/C9 paragonite/phengite


SiO2TiO2Al2O3Fe2O3FeOMgONa2OK2O

H2Ototal

SiAlt

AloTiFe3

Fe2Mg

NaK

sum

OH

Mg/(Mg+Fe)Na/(Na+K)

Bk 10B6318.10.93large core

51,720,1724,491,130,684,590,3810,57

4,4398,16

3,4920,508

1,4400,0090,0581,506

0,0380,4620,500

0,0500,9300,980

6,987

2

0,830,05

Bk 10B6418.10.93large core

52,230,1924,961,160,734,560,3210,71

4,4899,34

3,4850,515

1,4470,0100,0581,515

0,0410,4530,494

0,0410,9310,973

6,982

2

0,820,04

Bk 10B2719.10.93bsmall

50,120,3027,891,520,193,580,6710,15

4,4798,88

3,3520,648

1,5510,0150,0761,642

0,0100,3570,367

0,0870,8850,972

6,981

2

0,800,09


49,210,1727,691,920,163,330,6910,21

4,4097,78

3,3370,663

1,5500,0090,0981,657

0,0090,3370,346

0,0910,9020,993

6,995

2

0,760,09


49,270,2327,641,830,003,480,6310,29

4,4197,78

3,3390,661

1,5460,0120,0941,651

0,0000,3510,351

0,0830,9090,992

6,994

2

0,790,08


49,350,2127,991,890,003,460,6610,16

4,4298,14

3,3280,672

1,5530,0110,0961,659

0,0000,3480,348

0,0860,8930,979

6,986

2

0,780,09


49,180,3527,911,650,023,420,6210,36

4,4197,92

3,3280,672

1,5540,0180,0841,656

0,0010,3450,346

0,0810,9140,995

6,997

2

0,800,08

Bk 74526.4.93i (grt)

48,560,2027,862,620,003,260,899,95

4,3897,73

3,2970,703

1,5270,0100,1341,671

0,0000,3300,330

0,1170,8810,998

6,998

2

0,710,12

Bk 74626.4.93i (grt)

48,220,2027,363,410,003,720,909,77

4,3797,96

3,2640,736

1,4470,0100,1741,631

0,0000,3750,375

0,1180,8620,980

6,987

2

0,680,12

Bk 74826.4.93i (grt)

48,890,1727,841,880,522,990,9210,19

4,3997,79

3,3240,676

1,5550,0090,0961,659

0,0300,3030,333

0,1210,9031,024

7,016

2

0,710,12

Bk 75026.4.93i (grt)

49,210,1828,102,700,003,170,8710,16

4,4398,82

3,3090,691

1,5350,0090,1371,681

0,0000,3180,318

0,1130,8901,004

7,002

2

0,700,11

sampleanalysisdate


H2O

Si

AloFe3

MgCa

NaK

sum

OH


Bk 94724.2.94

45,6540,480,570,070,217,340,3994,71

4,67

2,933

3,0650,0273,093

0,0070,0140,021

0,9140,0330,947

4,137

2

Bk 94824.2.94

47,1340,870,410,090,237,420,3696,51

4,76

2,966

3,0310,0193,051

0,0080,0160,024

0,9050,0300,935

4,073

2

Bk 95224.2.94

49,1038,670,480,130,247,130,5796,32

4,77

3,089

2,8670,0232,890

0,0120,0160,028

0,8700,0470,916

3,909

2

Bk 93230.6.94

46,6139,690,360,130,247,310,6294,96

4,68

2,986

2,9960,0173,013

0,0120,0160,029

0,9080,0520,960

4,065

2

Bk 93330.6.94

46,4939,200,360,170,217,300,7794,50

4,65

2,995

2,9760,0172,994

0,0160,0140,031

0,9120,0650,977

4,066

2

Bk 93430.6.94

46,4439,320,480,130,257,450,3194,38

4,66

2,991

2,9840,0233,007

0,0120,0170,030

0,9300,0260,956

4,069

2

Bk 93530.6.94

46,8338,960,280,210,217,210,5894,28

4,65

3,017

2,9580,0132,971

0,0200,0140,035

0,9010,0490,949

4,017

2

Cig 91-12717.6.93

47,3039,411,000,270,116,661,4896,23

4,73

3,002

2,9480,0482,995

0,0260,0070,033

0,8190,1220,942

4,099

2

Cig 91-13117.6.93

47,3439,451,070,340,167,091,4196,86

4,75

2,991

2,9380,0512,988

0,0320,0110,043

0,8690,1160,985

4,160

2

Cig 91-13517.6.93

48,0538,171,120,790,146,571,3696,20

4,73

3,048

2,8530,0542,907

0,0750,0100,084

0,8080,1120,920

4,103

2

Cig 91-13617.6.93

48,2137,901,070,880,136,341,6296,15

4,72

3,060

2,8360,0512,887

0,0830,0090,092

0,7800,1340,914

4,087

2

normed on 11 oxygen, Fe3 estimated over Fetot - (Si-Mg-3) iterativ

Position means analysis of: large core, core of large phengite; large rim, rim of large phengite: large c-r, undefinedposition in a large phengite; small, a small phengite; i(grt), phengite inclusion in garnet

C-38 Appendix C Table C9 phengite




H2Ototal

SiAlt

AloTiFe3

Fe2Mg

NaK

sum

OH

Mg/(Mg+Fe)Na/(Na+K)




H2Ototal

SiAlt

AloTiFe3

Fe2Mg

NaK

sum

OH

Mg/(Mg+Fe)Na/(Na+K)


Bk 75426.4.93i (grt)

49,330,2228,292,200,353,020,9810,25

4,4599,09

3,3100,690

1,5480,0110,1111,670

0,0200,3020,322

0,1280,8971,024

7,016

2

0,700,12

Bk 75526.4.93i (grt)

49,740,2127,921,610,563,210,8110,30

4,4598,80

•

3,3420,658

1,5530,0110,0811,645

0,0310,3210,353

0,1060,9021,007

7,005

2

0,740,10

Bk 75626.4.93i (grt)

48,600,2128,822,040,002,950,8210,33

4,4198,19

3,2860,714

1,5820,0110,1041,697

0,0000,2970,297

0,1070,9101,018

7,012

2

0,740,11

Cig 91-17716.6.93small

49,890,3729,392,450,282,930,7710,22

4,53100,83

3,2850,715

1,5650,0180,1221,705

0,0160,2880,303

0,0980,8770,975

6,984

2

0,680,10

Cig 91-17816.6.93small

50,560,2428,762,130,373,210,7110,51

4,54101,03

3,3230,677

1,5510,0120,1051,668

0,0200,3140,335

0,0900,9000,991

6,994

2

0,710,09

Cig 91-1217.6.93small c

52,310,1824,670,960,764,630,3311,05

4,4899,37

3,4950,505

1,4370,0090,0481,495

0,0430,4610,504

0,0430,9621,005

7,003

2

0,840,04

Cig 91-1317.6.93small c

51,970,2024,841,170,604,560,3211,16

4,4799,29

3,4780,522

1,4380,0100,0591,507

0,0330,4550,488

0,0420,9731,015

7,010

2

0,830,04

Cig 91-1417.6.93small c

52,800,1624,800,631,254,500,3210,97

4,5199,94

3,5070,493

1,4480,0080,0321,488

0,0700,4460,515

0,0410,9500,991

6,994

2

0,820,04

Cig 91-1617.6.93small r

48,990,3528,342,860,412,840,8010,14

4,4499,17

3,2900,710

1,5330,0180,1451,695

0,0230,2840,308

0,1040,8870,992

6,994

2

0,630,11

Cig 91-1717.6.93small

49,580,2928,112,260,243,220,7010,36

4,4599,21

3,3200,680

1,5390,0150,1141,667

0,0130,3210,335

0,0910,9040,995

6,997

2

0,720,09

Cig 91-1817.6.93small

50,130,2027,612,420,103,500,6910,50

4,4799,62

3,3440,656

1,5140,0100,1211,646

0,0060,3480,354

0,0890,9131,002

7,001

2

0,730,09

Cig 91-1917.6.93small

48,690,3528,913,080,002,851,0110,35

4,4599,69

3,2550,745

1,5330,0180,1551,705

0,0000,2840,284

0,1310,9021,033

7,022

2

0,650,13

Cig 91-11017.6.93small

49,030,2628,523,000,003,140,8610,54

4,4699,81

•

3,2720,728

1,5150,0130,1511,678

0,0000,3120,312

0,1110,9171,028

7,019

2

0,670,11

Cig 91-11117.6.93small

50,300,2228,402,180,013,420,8510,41

4,51100,30

3,3270,673

1,5410,0110,1081,660

0,0010,3370,338

0,1090,8971,006

7,004

2

0,760,11

Cig 91-11217.6.93small

49,960,2127,812,480,003,590,8110,45

4,4899,78

3,3250,675

1,5060,0110,1241,640

0,0000,3560,356

0,1050,9061,011

7,007

2

0,740,10

Cig 91-11317.6.93small

50,150,2828,091,810,783,100,7010,66

4,49100,06

3,3370,663

1,5400,0140,0911,644

0,0430,3070,351

0,0900,9241,015

7,010

2

0,700,09

Cig 91-11417.6.93small

50,190,1927,652,290,263,430,7010,54

4,4799,72

3,3460,654

1,5180,0100,1151,643

0,0150,3410,355

0,0900,9161,006

7,004

2

0,720,09

Cig 91-11517.6.93small

49,810,1828,042,330,163,280,8410,44

4,4799,54

3,3260,674

1,5330,0090,1171,659

0,0090,3260,335

0,1090,9091,017

7,012

2

0,720,11

Cig 91-11917.6.93small

49,570,2627,792,400,343,190,7610,50

4,4599,26

3,3250,675

1,5220,0130,1211,656

0,0190,3190,338

0,0990,9181,017

7,011

2

0,690,10

Cig 91-12017.6.93small

49,930,2928,711,870,453,090,6310,49

4,4999,96

3,3170,683

1,5640,0140,0941,672

0,0250,3060,331

0,0810,9080,989

6,993

2

0,720,08

Cig 91-12117.6.93large core

52,460,2125,151,700,364,640,2711,31

4,52100,62

3,4670,533

1,4250,0100,0841,520

0,0200,4570,477

0,0350,9741,009

7,006

2

0,810,03


52,240,2624,721,640,304,750,3211,26

4,4999,98

3,4740,526

1,4120,0130,0821,507

0,0160,4710,487

0,0410,9761,017

7,012

2

0,830,04

C-39Appendix C Table C9 phengite




H2Ototal

SiAlt

AloTiFe3

Fe2Mg

NaK

sum

OH

Mg/(Mg+Fe)Na/(Na+K)




H2Ototal

SiAlt

AloTiFe3

Fe2Mg

NaK

sum

OH

Mg/(Mg+Fe)Na/(Na+K)



52,520,2424,610,980,864,630,2911,29

4,5099,92

3,4950,505

1,4260,0120,0491,487

0,0480,4590,507

0,0370,9791,017

7,011

2

0,830,04


52,350,2424,781,380,504,700,2611,19

4,4999,89

3,4820,518

1,4240,0120,0691,505

0,0280,4660,494

0,0340,9701,003

7,002

2

0,830,03


51,760,1924,250,820,844,580,3211,14

4,4398,33

3,4990,501

1,4320,0100,0421,483

0,0480,4620,509

0,0420,9821,024

7,016

2

0,840,04


51,130,1824,380,841,024,340,3210,63

4,3897,22

3,4900,510

1,4520,0090,0431,504

0,0580,4420,500

0,0420,9460,988

6,992

2

0,810,04

Cig 91-11928.11.93large c-r

50,660,2225,561,660,294,180,4310,75

4,4298,17

3,4270,573

1,4650,0110,0851,561

0,0170,4210,438

0,0560,9481,004

7,003

2

0,810,06

Cig 91-12028.11.93large c-r

50,920,3025,140,960,874,150,4210,82

4,4197,99

3,4540,546

1,4630,0150,0491,527

0,0490,4200,469

0,0550,9561,012

7,008

2

0,810,05

Cig 91-12228.11.93large c-r

50,770,2425,400,451,263,900,4510,76

4,4097,64

3,4550,545

1,4920,0120,0231,528

0,0720,3960,467

0,0590,9541,014

7,009

2

0,810,06

Cig 91-12328.11.93large c-r

50,660,1826,021,050,633,960,4010,84

4,4298,17

3,4260,574

1,5000,0090,0531,562

0,0360,3990,435

0,0520,9551,008

7,005

2

0,820,05


51,380,1824,430,721,144,320,3910,71

4,4097,67

3,4930,507

1,4510,0090,0371,497

0,0650,4380,503

0,0510,9491,000

7,000

2

0,810,05


51,630,2124,190,591,264,400,2510,91

4,4197,85

3,5060,494

1,4430,0110,0301,483

0,0720,4450,517

0,0330,9660,999

6,999

2

0,810,03

Cig 91-12628.11.93large rim

50,330,2026,732,450,103,701,3110,28

4,4699,57

3,3640,636

1,4700,0100,1231,604

0,0060,3690,374

0,1700,8961,065

7,044

2

0,740,16

Cig 91-12828.11.93large c-r

51,050,1925,890,641,283,790,6210,53

4,4498,43

3,4440,556

1,5020,0100,0331,544

0,0720,3810,453

0,0810,9261,007

7,005

2

0,780,08


51,770,2124,290,841,014,500,2411,00

4,4398,29

3,5000,500

1,4360,0110,0431,489

0,0570,4530,511

0,0310,9691,001

7,000

2

0,820,03


49,960,2127,771,890,273,400,6110,76

4,4699,33

3,3440,656

1,5340,0110,0951,640

0,0150,3390,354

0,0790,9391,018

7,012

2

0,750,08


52,330,2025,090,801,004,410,2911,28

4,5099,90

3,4830,517

1,4510,0100,0401,502

0,0560,4380,493

0,0370,9791,016

7,011

2

0,820,04


48,620,3628,672,690,072,890,7610,21

4,4298,69

3,2760,724

1,5530,0180,1361,707

0,0040,2900,294

0,0990,8970,996

6,997

2

0,670,10


49,480,3528,121,940,583,060,7810,26

4,4599,02

3,3210,679

1,5460,0180,0981,661

0,0330,3060,339

0,1020,8980,999

6,999

2

0,700,10

Cig 91-14217.6.93small

50,350,2227,431,760,463,491,0410,19

4,4799,41

3,3620,638

1,5210,0110,0881,620

0,0260,3470,373

0,1350,8871,021

7,014

2

0,750,13


50,580,2628,441,410,723,220,7010,53

4,52100,38

3,3440,656

1,5610,0130,0701,644

0,0400,3170,357

0,0900,9070,997

6,998

2

0,740,09


49,270,2927,591,190,933,070,6210,40

4,4097,76

3,3490,651

1,5590,0150,0611,635

0,0530,3110,364

0,0820,9211,003

7,002

2

0,730,08


51,710,2124,510,661,264,320,2710,94

4,4398,31

3,4960,504

1,4490,0110,0341,494

0,0710,4350,507

0,0350,9640,999

7,000

2

0,810,04


51,430,2224,150,780,944,500,2711,05

4,4097,74

3,4980,502

1,4340,0110,0401,486

0,0530,4560,509

0,0360,9801,015

7,010

2

0,830,04

C-40 Appendix C Table C9/C10 phengite/rutile



H2Ototal

SiAlt

AloTiFe3

Fe2Mg

NaK

sum

OH

Mg/(Mg+Fe)Na/(Na+K)



Cig 91-1.2542.7.94large core

51,990,1824,840,900,814,520,3910,68

4,4698,77

3,4890,511

1,4530,0090,0451,507

0,0460,4520,498

0,0510,9340,985

6,990

2

0,830,05

SampleDateNr

TiO2Fe2O3

sum

TiFe3

Bk 10B19.10.935

97,000,59

97,59

0,9940,006

Bk 10B19.10.936

98,830,46

99,29

0,9950,005

Bk 186.8.941

99,700,57

100,27

0,9940,006

Bk 392.7.9420

97,870,77

98,64

0,9920,008

Bk 392.7.9421

98,090,77

98,86

0,9920,008

Bk 395.5.9212

98,090,58

98,67

0,9940,006

Bk 39.128.8.9215

99,020,66

99,68

0,9930,007

Bk 39a28.1.9327

98,621,04

99,66

0,9900,010

Bk 39a28.1.9330

98,570,73

99,30

0,9930,007

Bk 730.6.9453

98,230,42

98,65

0,9960,004

Bk 76.7.9242

98,50,63

99,13

0,9940,006

Bk 76.7.9270

98,170,47

98,64

0,9950,005

SampleDateNr

TiO2Fe2O3

sum

TiFe3

Bk 814.3.9345

97,120,71

97,83

0,9930,007

Bk 829.1.931

97,720,54

98,26

0,9950,005

Bk 829.1.932

98,050,62

98,67

0,9940,006

Bk 829.1.934,2

97,360,63

97,99

0,9940,006

Bk 829.1.936,2

96,60,60

97,20

0,9940,006

Bk 829.1.9316,2

98,420,81

99,23

0,9920,008

Bk 924.2.942

98,40,49

98,89

0,9950,005

Bk 924.2.943

96,60,62

97,22

0,9940,006

Bk 924.2.9477

97,410,40

97,81

0,9960,004

Bk 924.2.9478

990,44

99,44

0,9960,004

Bk 930.6.9423

98,240,47

98,71

0,9950,005

Cig 91-1.2552.7.94large rim

49,520,2627,331,710,453,380,6810,26

4,4198,00

3,3530,647

1,5350,0130,0871,635

0,0250,3410,367

0,0890,9060,995

6,997

2

0,750,09

Cig 91-1.213.7.94large rim

50,600,2227,321,310,843,490,5910,27

4,4799,11

3,3840,616

1,5370,0110,0661,614

0,0470,3480,395

0,0770,8950,972

6,981

2

0,750,08

Cig 91-1.223.7.94large c-r

51,890,2124,030,750,964,660,2910,68

4,4297,89

3,5140,486

1,4320,0110,0381,481

0,0550,4700,525

0,0380,9430,981

6,987

2

0,840,04


52,010,2124,460,690,744,700,3910,70

4,4498,34

3,5030,497

1,4440,0110,0351,490

0,0420,4720,513

0,0510,9390,990

6,993

2

0,860,05


52,240,1924,400,850,734,730,4310,78

4,4698,82

3,5050,495

1,4340,0100,0431,486

0,0410,4730,514

0,0560,9430,998

6,999

2

0,850,06


51,190,2025,041,240,784,260,3610,57

4,4298,05

3,4630,537

1,4600,0100,0631,533

0,0440,4300,474

0,0470,9320,979

6,986

2

0,800,05


52,020,1624,450,511,224,470,3110,65

4,4498,23

3,5100,490

1,4550,0080,0261,489

0,0690,4500,519

0,0410,9370,977

6,985

2

0,830,04


51,650,1524,230,761,084,460,3710,74

4,4197,85

3,5040,496

1,4420,0080,0391,488

0,0610,4510,512

0,0490,9500,998

6,999

2

0,820,05

SampleDateNr

TiO2Fe2O3

sum

TiFe3

Bk 930.6.9423

98,290,46

98,75

0,9950,005

Cig 91.1.22.7.9413

98,890,56

99,45

0,9940,006

normed on 1cation

normed on 1cation

normed on 1cation

C-41Appendix C Table C11/C12 dolomite/calcite

normed on 2 cations

normed on 1cation

Bk766.7.92

33,9017,408,340,5660,20

51,06111,26

1,042

0,7440,2000,0140,958

2

normed on 2 cations


CaMgFeMn

CO2total

Ca

MgFeMn

CO3

Bk 7726.4.93yellow

52,391,972,130,65

44,97102,11

0,914

0,0480,0290,009

1

Bk 7826.4.93brown

50,902,552,410,65

44,61101,12

0,895

0,0620,0330,009

1

Bk 72126.4.93yellow

51,102,392,190,56

44,40100,64

0,903

0,0590,0300,008

1

Bk 72226.4.93yellow

50,552,432,450,53

44,15100,11

0,898

0,0600,0340,007

1

Bk 76326.4.93yellow

53,281,311,470,63

44,53101,22

0,939

0,0320,0200,009

1

Bk 76426.4.93yellow

51,921,301,570,57

43,4898,84

0,937

0,0330,0220,008

1

Bk 726.7yellow

63,611,241,400,86

52,66119,77

0,948

0,0260,0160,010

1

Bk 746.7yellow

62,281,682,111,06

52,66119,79

0,928

0,0350,0250,012

1

Bk 7106.7orange

59,982,182,721,29

51,92118,09

0,907

0,0460,0320,015

1

Bk 7336.7yellow

62,601,011,871,07

52,04118,59

0,944

0,0210,0220,013

1


54,901,851,200,64

46,24104,83

0,932

0,0440,0160,009

1


54,281,771,540,68

45,90104,17

0,928

0,0420,0210,009

1

sampleanalysisdate

CaMgFeMnsum

CO2total

Ca

MgFeMn

CO3

Bk7526.4.93

29,6715,697,790,4053,55

45,4398,98

1,025

0,7540,2100,0110,975

2

Bk7626.4.93

29,9015,987,590,4153,88

45,8199,69

1,024

0,7620,2030,0110,976

2

Bk7926.4.93

29,3215,437,810,4753,03

44,9397,96

1,024

0,7500,2130,0130,976

2

Bk71026.4.93

33,3413,186,910,5653,99

45,1399,12

1,159

0,6380,1880,0150,841

2

Bk71126.4.93

29,9515,688,040,5454,21

45,88100,09

1,025

0,7460,2150,0150,975

2

Bk71226.4.93

30,3415,437,600,5153,88

45,6399,51

1,044

0,7380,2040,0140,956

2

Bk72326.4.93

29,6114,628,550,4053,18

44,6897,86

1,040

0,7140,2340,0110,960

2

Bk72426.4.93

29,5115,757,960,4153,63

45,4899,11

1,018

0,7560,2140,0110,982

2

Bk75926.4.93

29,4515,537,920,5453,44

45,2598,69

1,021

0,7490,2140,0150,979

2

Bk76026.4.93

29,4616,047,560,4353,49

45,5399,02

1,016

0,7690,2030,0120,984

2

Bk796.7.92

33,2616,818,820,6159,50

50,24109,74

1,039

0,7310,2150,0150,961

2

Bk7346.7.92

32,6117,528,840,6359,60

50,52110,12

1,013

0,7570,2140,0150,987

2

sampleanalysisdate

CaMgFeMnsum

CO2total

Ca

MgFeMn

CO3


CaMgFeMn

CO2total

Ca

MgFeMn

CO3


53,651,971,850,73

45,84104,04

0,918

0,0470,0250,010

1


51,421,751,430,50

43,4598,55

0,929

0,0440,0200,007

1


51,381,832,120,96

44,21100,50

0,912

0,0450,0290,013

1


52,791,962,520,82

45,62103,71

0,908

0,0470,0340,011

1


51,541,301,770,72

43,4098,73

0,932

0,0330,0250,010

1


52,911,261,730,71

44,40101,01

0,935

0,0310,0240,010

1


49,871,661,960,74

42,6196,84

0,919

0,0430,0280,011

1


50,591,621,900,68

43,0697,85

0,922

0,0410,0270,010

1


50,051,701,800,69

42,6696,90

0,921

0,0440,0260,010

1


50,211,411,790,54

42,3796,32

0,930

0,0360,0260,008

1

normed on 1cation

C-42 Appendix C Table C12 calcite


CaMgFeMn

CO2total

Ca

MgFeMn

CO3

normed on 1cation


CaMgFeMn

CO2total

Ca

MgFeMn

CO3

normed on 1cation


CaMgFeMn

CO2total

Ca

MgFeMn

CO3

normed on 1cation


CaMgFeMn

CO2total

Ca

MgFeMn

CO3

normed on 1cation


50,981,601,940,70

43,3898,60

0,922

0,0400,0270,010

1


50,371,641,790,66

42,8397,29

0,923

0,0420,0260,010

1


50,521,601,930,60

42,9597,60

0,923

0,0410,0280,009

1


51,271,511,690,68

43,3498,49

0,928

0,0380,0240,010

1


53,030,720,750,69

43,2998,48

0,961

0,0180,0110,010

1


52,140,980,970,65

42,9997,73

0,952

0,0250,0140,009

1


53,130,710,730,62

43,3098,49

0,963

0,0180,0100,009

1


51,721,330,930,55

42,9597,48

0,945

0,0340,0130,008

1


52,471,220,980,75

43,5899,00

0,945

0,0310,0140,011

1


52,241,000,870,58

42,9897,67

0,954

0,0250,0120,008

1


53,380,720,920,56

43,5999,17

0,961

0,0180,0130,008

1


51,471,601,450,70

43,4698,68

0,929

0,0400,0200,010

1


51,191,521,290,71

43,0697,77

0,933

0,0390,0180,010

1


52,241,431,460,64

43,8599,62

0,935

0,0360,0200,009

1


51,581,411,190,52

43,0797,77

0,940

0,0360,0170,007

1


52,051,401,160,64

43,4898,73

0,939

0,0350,0160,009

1

Bk 95223.2.94

64,320,790,630,30

51,91117,95

0,972

0,0170,0070,004

1

Bk 93024.2.94

63,380,220,760,28

50,62115,26

0,983

0,0050,0090,003

1

Bk 93124.2.94

64,310,180,650,25

51,22116,61

0,985

0,0040,0080,003

1

Bk 93224.2.94

62,370,741,170,51

50,79115,58

0,964

0,0160,0140,006

1

Bk 9424.2.94

62,150,641,140,44

50,44114,81

0,967

0,0140,0140,005

1

Bk 93524.2.94

63,080,280,660,37

50,44114,83

0,981

0,0060,0080,005

1

Bk 93624.2.94

61,350,430,660,24

49,17111,85

0,979

0,0100,0080,003

1

Bk 9144.3.94

63,480,600,670,34

51,09116,18

0,975

0,0130,0080,004

1

Bk 9154.3.94

63,990,440,650,37

51,33116,78

0,978

0,0090,0080,004

1

Bk 9174.3.94

65,160,891,310,37

53,14120,87

0,962

0,0180,0150,004

1

Bk 9184.3.94

65,040,781,280,41

52,93120,44

0,964

0,0160,0150,005

1


57,010,380,430,41

45,67103,90

0,980

0,0090,0060,006

1


54,980,370,540,48

44,18100,55

0,977

0,0090,0070,007

1


54,810,290,390,43

43,8499,76

0,981

0,0070,0050,006

1


53,110,750,640,41

43,1498,05

0,966

0,0190,0090,006

1


54,260,190,450,41

43,3298,63

0,983

0,0050,0060,006

1


53,710,240,380,41

42,9097,64

0,983

0,0060,0050,006

1


54,350,280,400,33

43,4198,77

0,983

0,0070,0060,005

1


49,401,691,980,74

42,2996,10

0,917

0,0440,0290,011

1


51,131,341,570,59

42,9297,55

0,935

0,0340,0220,009

1


49,921,762,270,62

42,8797,44

0,914

0,0450,0320,009

1


50,641,711,940,70

43,2398,22

0,919

0,0430,0270,010

1


50,641,752,130,67

43,3798,56

0,916

0,0440,0300,010

1


50,921,381,970,60

43,0597,92

0,928

0,0350,0280,009

1


50,631,502,020,46

42,8997,50

0,926

0,0380,0290,007

1


52,621,051,600,55

43,7699,58

0,944

0,0260,0220,008

1


50,631,502,020,46

42,8997,50

0,926

0,0380,0290,007

1


52,621,051,600,55

43,7699,58

0,944

0,0260,0220,008

1

C-43Appendix C Table C12/C13 calcite/albite

normed on 1cation


SiO2Al2O3Fe2O3CaOBaONa2OK2OTotal

SiAlFe3

CaBaNaK

sum

An%

Bk 10B518.10.93sympl

69,3720,060,260,500,0311,270,07101,56

2,9791,0150,0204,014

0,0230,0010,9380,0040,966

4,980

2,382

Bk 10B1318.10.93sympl

70,3220,250,230,190,0010,660,08101,73

2,9991,0180,0184,036

0,0090,0000,8820,0040,895

4,930

0,970

Bk 10B4518.10.93sympl

67,4519,800,180,681,3110,830,10100,35

2,9631,0250,0134,002

0,0320,0230,9220,0060,983

4,984

3,257


68,7619,700,440,560,0111,060,05100,58

2,9781,0060,0344,018

0,0260,0000,9290,0030,958

4,976

2,713

Bk 173913.7.94sympl

67,6419,650,040,220,0310,980,0598,61

2,9891,0230,0034,016

0,0100,0010,9410,0030,955

4,970

1,091

Bk 174113.7.94sympl

67,9420,080,080,620,0011,060,0799,85

2,9701,0350,0064,011

0,0290,0000,9380,0040,971

4,981

2,992

Bk 174213.7.94grt ps

66,3121,200,101,930,0310,440,07100,08

2,9061,0950,0084,008

0,0910,0010,8870,0040,982

4,990

9,226

Bk 174313.7.94grt ps

66,3320,870,071,720,0010,350,0799,41

2,9221,0830,0054,010

0,0810,0000,8840,0040,969

4,979

8,376

Bk 174413.7.94grt ps

66,0121,140,031,970,0010,280,1099,53

2,9081,0980,0034,008

0,0930,0000,8780,0060,977

4,985

9,519

Bk 174613.7.94sympl

68,0919,790,120,670,0011,060,0699,79

2,9781,0200,0094,007

0,0310,0000,9380,0030,973

4,980

3,228

Bk 17563.7.94sympl

68,4019,980,210,500,1811,250,03100,55

2,9721,0230,0164,011

0,0230,0030,9480,0020,976

4,987

2,385

Bk 17573.7.94sympl

67,8919,720,080,470,0310,780,0599,02

2,9871,0230,0064,016

0,0220,0010,9200,0030,945

4,961

2,344

normed on 8 oxygen, all Fe assumed Fe3


CaMgFeMn

CO2total

Ca

MgFeMn

CO3


53,720,460,540,35

43,2198,28

0,976

0,0120,0080,005

1


53,400,340,550,35

42,8397,47

0,978

0,0090,0080,005

1


53,770,330,550,35

43,1198,11

0,979

0,0080,0080,005

1


53,340,620,850,57

43,4198,79

0,964

0,0160,0120,008

1


53,500,510,610,40

43,1698,18

0,973

0,0130,0090,006

1


53,590,320,790,48

43,1998,37

0,974

0,0080,0110,007

1


54,460,530,570,26

43,8399,65

0,975

0,0130,0080,004

1


53,350,260,500,38

42,6997,18

0,981

0,0070,0070,006

1


54,100,250,490,37

43,2698,47

0,981

0,0060,0070,005

1


53,850,260,390,41

43,0497,95

0,982

0,0070,0060,006

1



SiAlFe3

CaBaNaK

sum

An%


Bk 17583.7.94sympl

67,6919,700,080,350,0611,320,0699,26

2,9791,0220,0064,006

0,0170,0010,9660,0030,987

4,993

1,672

Bk 17593.7.94sympl

66,3420,650,121,420,0010,200,0598,78

2,9341,0760,0094,019

0,0670,0000,8750,0030,945

4,964

7,122

Bk 17603.7.94sympl

68,1419,820,170,480,0311,170,0499,85

2,9781,0210,0134,011

0,0220,0010,9460,0020,972

4,983

2,313

Bk 17613.7.94sympl

66,1320,490,121,430,0910,460,0698,78

2,9311,0700,0094,010

0,0680,0020,8990,0030,972

4,982

6,988

Bk 17623.7.94sympl

68,1619,620,060,290,0011,190,0699,38

2,9911,0150,0044,009

0,0140,0000,9520,0030,969

4,978

1,407

Bk 17633.7.94sympl

68,2519,530,040,260,0511,360,0399,52

2,9921,0090,0034,005

0,0120,0010,9660,0020,981

4,986

1,246

Bk 17643.7.94sympl

68,2819,630,070,210,0111,150,0599,40

2,9931,0140,0054,013

0,0100,0000,9480,0030,961

4,973

1,027

Bk 1739.7.94sympl

66,9320,330,341,250,0210,790,0399,69

2,9351,0510,0264,013

0,0590,0000,9180,0020,978

4,991

6,004

Bk 17149.7.94sympl

68,7419,760,070,310,0011,380,05100,31

2,9891,0130,0054,007

0,0140,0000,9600,0030,977

4,984

1,479

Bk 17159.7.94sympl

68,3419,950,060,370,0011,280,02100,02

2,9811,0260,0044,010

0,0170,0000,9540,0010,972

4,983

1,778

position: sympl is albite in symplectite, grt ps is albite in chlorite albite epidoze aggregates after garnet,vein is albite in veins

C-44 Appendix C Table C13 albite




SiAlFe3

CaBaNaK

sum

An%


Bk 17169.7.94vein

66,4521,270,081,820,0010,460,06100,14

2,9081,0970,0064,011

0,0850,0000,8880,0030,976

4,987

8,741

Bk 17179.7.94vein

66,1920,970,081,820,0010,420,0399,51

2,9141,0880,0064,008

0,0860,0000,8900,0020,977

4,985

8,787

Bk 17189.7.94vein

66,6520,830,081,650,0010,550,0799,83

2,9241,0770,0064,007

0,0780,0000,8970,0040,979

4,986

7,923

Bk 17199.7.94vein

66,5320,920,111,670,0510,440,0499,76

2,9201,0820,0084,011

0,0790,0010,8890,0020,970

4,981

8,095

Bk 17209.7.94vein

67,4520,380,131,220,0110,890,04100,12

2,9471,0490,0104,006

0,0570,0000,9220,0020,982

4,988

5,815

Bk 17219.7.94vein

66,4720,700,141,670,0010,410,0699,45

2,9251,0740,0114,010

0,0790,0000,8880,0030,970

4,980

8,114

Bk 17229.7.94sympl

68,6319,610,210,110,0011,340,0399,93

2,9911,0070,0164,015

0,0050,0000,9580,0020,965

4,980

0,532

Bk 17239.7.94sympl

68,9419,580,090,050,0011,260,0299,94

3,0031,0050,0074,015

0,0020,0000,9510,0010,954

4,969

0,244

Bk 17529.7.94sympl

68,5219,390,100,090,0011,270,0299,39

3,0021,0010,0084,011

0,0040,0000,9570,0010,963

4,974

0,439

Bk 17539.7.94sympl

68,7719,530,200,130,0011,500,02100,15

2,9931,0020,0154,010

0,0060,0000,9700,0010,978

4,988

0,620

Bk 18175.8.94sympl

67,9720,290,130,840,0010,620,0399,88

2,9661,0440,0104,020

0,0390,0000,8990,0020,940

4,959

4,180



SiAlFe3

CaBaNaK

sum

An%


Bk 18185.8.94sympl

68,6820,080,330,280,0110,900,11100,39

2,9771,0260,0264,029

0,0130,0000,9160,0060,935

4,964

1,390

Bk 391113.3.93sympl

69,0220,100,000,360,0011,500,02101,00

2,9831,0240,0004,006

0,0170,0000,9640,0010,981

4,988

1,699

Bk 393313.3.93sympl

67,8219,440,290,440,1811,570,0399,77

2,9741,0050,0224,001

0,0210,0030,9840,0021,009

5,010

2,048

Bk 395424.6.92sympl

69,1320,080,210,170,0211,160,01100,78

2,9851,0220,0164,024

0,0080,0000,9340,0010,943

4,967

0,834

Bk 395524.6.92sympl

68,2219,850,520,510,1110,570,0299,80

2,9731,0200,0404,033

0,0240,0020,8930,0010,920

4,953

2,589

Bk 395924.6.92sympl

68,3820,230,290,290,0511,270,02100,53

2,9661,0340,0224,022

0,0130,0010,9480,0010,963

4,985

1,399

Bk 396024.6.92sympl

66,6920,610,260,930,0010,830,0299,34

2,9331,0680,0194,021

0,0440,0000,9230,0010,968

4,989

4,525

Bk 3965.5.92sympl

67,2419,350,400,540,0511,260,0298,86

2,9701,0070,0304,008

0,0260,0010,9640,0010,992

4,999

2,576

Bk 39.12128.8.92sympl

67,2819,880,080,610,1011,460,0099,41

2,9631,0320,0064,000

0,0290,0020,9780,0001,009

5,009

2,852

Bk 39.12528.8.92sympl

68,8019,750,120,310,0011,460,03100,47

2,9871,0110,0094,007

0,0140,0000,9650,0020,981

4,988

1,470

Bk 39.12628.8.92sympl

69,2120,760,060,360,0010,580,03101,00

2,9781,0530,0044,035

0,0170,0000,8830,0020,901

4,936

1,842



SiAlFe3

CaBaNaK

sum

An%


Bk 39.14528.8.92sympl

68,8019,480,930,840,0010,140,03100,22

2,9770,9930,0724,042

0,0390,0000,8510,0020,891

4,933

4,369

Bk 72727.8.92sympl

68,2020,940,220,440,0511,140,04101,03

2,9451,0660,0174,028

0,0200,0010,9330,0020,956

4,985

2,129

Bk 73627.8.92sympl

68,9020,960,090,540,0010,750,05101,29

2,9621,0620,0074,031

0,0250,0000,8960,0030,924

4,955

2,693

Bk 81314.3.93sympl

68,4820,340,580,870,0010,080,23100,58

2,9601,0360,0454,041

0,0400,0000,8450,0130,898

4,939

4,487

Bk 86014.3.93sympl

69,0818,750,780,740,039,870,0599,30

3,0120,9640,0604,035

0,0350,0010,8340,0030,872

4,908

3,963

Bk 9252.7.94sympl

67,4519,990,070,700,0010,890,0799,17

2,9691,0370,0054,011

0,0330,0000,9290,0040,966

4,978

3,416

Bk 9262.7.94sympl

67,5120,180,090,910,0010,980,0699,73

2,9581,0420,0074,007

0,0430,0000,9330,0030,979

4,987

4,364

Bk 91724.2.94sympl

68,5820,120,220,480,0111,010,04100,46

2,9741,0290,0174,020

0,0220,0000,9260,0020,951

4,971

2,346

Bk 91824.2.94sympl

68,6820,150,280,230,0911,090,09100,61

2,9751,0290,0214,025

0,0110,0020,9310,0050,949

4,973

1,125

Bk 91924.2.94sympl

68,6220,100,100,250,0511,310,05100,48

2,9791,0280,0084,015

0,0120,0010,9520,0030,967

4,982

1,202

Bk 92024.2.94sympl

68,7020,030,210,270,0011,230,04100,48

2,9791,0240,0164,019

0,0130,0000,9440,0020,959

4,978

1,308

C-45Appendix C Table C13/C14 albite/amphibolearound garnet



sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name

amphibole names after Leake (1978): ed-hbl is edenitic-hornblende, fer-act-hbl is ferro-actinolitic-hornblende, fer-par is ferroan-pargasite, fer-par-hbl is ferroan-pargasitic-hornblende, mag-has is magnesian-hastingite, mag-hst-hbl ismagnesian-hastingitic-hornblende, tscherm is tschermakite

Bk 10 B819.10.93b

41,310,1211,750,0010,3213,920,236,679,280,272,880,68

1,9699,39

6,3201,680

0,4391,1890,0000,0101,5211,7810,0300,031

1,5210,4792,000

0,3760,1360,511

15,511

2

mag-hst-hbl



SiAlFe3

CaBaNaK

sum

An%

Bk 92124.2.94sympl

68,4820,120,260,410,0010,990,05100,30

2,9741,0300,0204,023

0,0190,0000,9250,0030,947

4,970

2,014

Bk 92224.2.94sympl

69,5320,100,190,150,0011,310,04101,32

2,9881,0180,0154,020

0,0070,0000,9420,0020,951

4,972

0,726

Bk 92324.2.94sympl

68,6920,030,170,240,1011,290,05100,57

2,9791,0240,0134,016

0,0110,0020,9490,0030,965

4,981

1,156

Cig91-13417.6.93sympl

64,2121,283,030,850,0010,030,1499,54

2,7981,0930,2324,123

0,0400,0000,8470,0080,895

5,017

4,434

Bk 10 B919.10.93b

40,900,0611,740,0210,1314,730,166,379,370,182,900,72

1,9599,22

6,2931,707

0,4231,1730,0020,0051,4611,8950,0210,020

1,5450,4552,000

0,4100,1440,554

15,554

2

mag-hst-hbl

Bk 10 B1019.10.93b

39,390,0813,990,0010,0513,850,276,089,700,332,740,88

1,9599,32

6,0521,948

0,5861,1620,0000,0071,3921,7800,0350,037

1,5970,4032,000

0,4130,1760,589

15,589

2

mag-has

Bk 10 B1519.10.93b

41,240,0212,210,0210,0213,760,236,799,370,042,790,70

1,9699,16

6,3031,697

0,5031,1530,0020,0021,5471,7590,0300,005

1,5340,4662,000

0,3610,1390,501

15,501

2

mag-hst-hbl

Bk 10 B326.11.93

38,380,1714,860,009,1215,240,215,309,740,252,821,04

1,9399,07

5,9502,050

0,6651,0640,0000,0141,2251,9760,0280,029

1,6180,3822,000

0,4650,2100,676

15,676

2

mag-has

Bk 10 B526.11.93

41,530,1712,850,018,3514,170,206,649,520,192,460,84

1,9698,89

6,3431,657

0,6570,9590,0010,0141,5121,8100,0260,021

1,5580,4422,000

0,2860,1670,454

15,454

2

fer-act-hbl

Bk 10 B926.11.93

41,470,0211,930,008,3615,100,226,599,570,172,790,70

1,9598,87

6,3731,627

0,5340,9670,0000,0021,5091,9400,0290,019

1,5760,4242,000

0,4070,1400,547

15,547

2

mag-hst-hbl

Bk 10 B1626.11.93

39,940,1113,830,007,6515,360,156,299,850,002,890,83

1,9598,84

6,1521,848

0,6620,8870,0000,0091,4441,9780,0200,000

1,6260,3742,000

0,4890,1670,655

15,655

2

mag-has

Bk 10 B1826.11.93

41,350,0614,210,027,7713,010,157,529,860,222,790,74

1,9999,69

6,2241,776

0,7450,8800,0020,0051,6871,6380,0190,024

1,5900,4102,000

0,4040,1450,549

15,549

2

mag-has

Bk 10 B1926.11.93

38,300,0515,920,017,4015,650,175,219,790,172,801,15

1,9398,54

5,9432,057

0,8540,8640,0010,0041,2052,0300,0220,019

1,6280,3722,000

0,4700,2330,702

15,702

2

mag-has

Bk 1895.8.94

41,160,2512,600,025,7915,820,287,4011,370,292,120,62

1,9799,69

6,2741,726

0,5380,6640,0020,0291,6812,0160,0360,033

1,8570,1432,000

0,4840,1230,607

15,607

2

mag-hst-hbl

normed on 23 oxygens, Fe3 over Si+Ti+Al+Fe+Mn+Mg+Ca+Zn = 13

C-46 Appendix C Table C14 amphibole aroundgarnet

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name

amphibole names after Leake (1978): ed-hbl is edenitic-hornblende, fer-act-hbl is ferro-actinolitic-hornblende, fer-par is ferroan-pargasite, fer-par-hbl is ferroan-pargasitic-hornblende, mag-has is magnesian-hastingite, mag-hst-hbl ismagnesian-hastingitic-hornblende, tscherm is tschermakite


sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Bk 18125.8.94

40,230,2212,540,0013,208,650,228,6610,300,151,740,51

1,9798,40

6,1131,887

0,3591,5100,0000,0251,9611,0990,0280,017

1,6770,3232,000

0,1900,1010,291

15,291

2

tscherm

Bk 392123.3.92

40,200,0313,060,005,4913,630,218,589,65n.a4,290,34

1,9497,42

6,2141,786

0,5930,6380,0000,0021,9771,7620,027 -

1,5980,4022,000

0,8840,0680,952

15,952

2

mag-has

Bk 392223.3.92

39,600,0613,670,016,7812,920,218,459,68n.a4,200,40

1,9597,93

6,0971,903

0,5780,7860,0010,0051,9391,6640,027 -

1,5970,4032,000

0,8510,0800,931

15,931

2

mag-has

Bk 392423.3.92

41,440,2214,910,002,7412,760,129,049,04n.a4,490,47

1,9797,19

6,3061,694

0,9790,3130,0000,0182,0501,6230,015 -

1,4740,5262,000

0,7980,0930,892

15,892

2

fer-par-hbl

Bk 7256.7.92

40,970,0815,730,033,6911,850,219,3110,10n.a3,740,41

1,9998,11

6,1701,830

0,9630,4180,0040,0062,0901,4920,027 -

1,6300,3702,000

0,7220,0800,802

15,802

2

fer-par

Bk 7117.7.92

43,270,1013,960,003,0014,110,208,198,68n.a4,160,47

1,9998,13

6,5251,475

1,0060,3400,0000,0081,8411,7800,026 -

1,4020,5982,000

0,6190,0920,711

15,711

2

ed-hbl

Bk 7137.7.92

44,880,1012,350,004,1112,810,139,458,68n.a4,170,31

2,0299,01

6,6691,331

0,8310,4590,0000,0082,0931,5920,016 -

1,3820,6182,000

0,5830,0600,643

15,643

2

ed-hbl

Bk 777.8.92

40,720,0515,480,035,5810,900,219,5810,070,164,000,31

2,0099,09

6,0911,909

0,8210,6280,0040,0042,1361,3640,0270,018

1,6140,3862,000

0,7740,0600,835

15,835

2

fer-par

Bk 787.8.92

43,080,1014,670,004,1510,440,1610,149,430,313,890,44

2,0298,83

6,3821,618

0,9430,4630,0000,0082,2391,2930,0200,034

1,4970,5032,000

0,6140,0850,699

15,699

2

fer-par-hbl

Bk 82414.3.93

41,240,0715,320,004,6613,490,287,729,380,113,840,43

1,9898,52

6,2381,762

0,9690,5300,0000,0061,7411,7060,0360,012

1,5200,4802,000

0,6460,0850,731

15,731

2

fer-par

Bk 82514.3.93

42,540,0013,460,045,5413,620,287,799,080,193,810,23

1,9898,57

6,4311,569

0,8300,6300,0050,0001,7551,7230,0360,021

1,4710,5292,000

0,5880,0450,633

15,633

2

fer-par-hbl

Bk 82814.3.93

41,650,0814,580,006,5513,090,327,429,090,253,770,33

1,9999,12

6,2771,723

0,8660,7430,0000,0061,6671,6490,0410,028

1,4680,5322,000

0,5690,0650,634

15,634

2

fer-par-hbl

Bk 82914.3.93

42,280,0713,960,036,4312,860,227,948,790,124,070,30

1,9999,06

6,3551,645

0,8280,7270,0040,0061,7791,6160,0280,013

1,4160,5842,000

0,6020,0590,660

15,660

2

fer-par-hbl

Cig 91-16817.6.93

41,160,0818,380,001,9514,520,177,189,070,004,420,61

2,0199,55

6,1281,872

1,3530,2180,0000,0061,5931,8070,0210,000

1,4470,5532,000

0,7230,1180,841

15,841

2

fer-par

Cig 91-16917.6.93

42,560,0617,090,003,0313,480,137,858,760,014,360,55

2,0399,92

6,2801,720

1,2510,3370,0000,0051,7261,6630,0160,001

1,3850,6152,000

0,6320,1060,738

15,738

2

fer-par-hbl

C-47Appendix C Table C15 amphibole aroundglaucophane

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name

amphibole names after Leake (1978): ac-hbl is actinolitic-hornblende, act is actinolite, barr is barroisite, ed isedenite, ed-hbl is edenitic-hornblende, mag-hbl is magnesio-hornblende, mag-kat is magnesio-katophorite


sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Bk 392924.6.92

49,330,1910,300,053,7911,340,089,625,35n.a.5,330,18

2,0497,60

7,2580,742

1,0440,4200,0060,0152,1101,3950,010-

0,8431,1572,000

0,3640,0350,398

15,398

2

barr

Bk 393724.6.92

50,480,1210,360,024,997,550,0711,334,81n.a.5,460,13

2,0797,39

7,3090,691

1,0770,5440,0020,0092,4450,9140,009-

0,7461,2542,000

0,2790,0250,303

15,303

2

barr

Bk 394024.6.92

46,850,109,660,023,359,470,1512,649,11n.a.3,810,23

2,0297,41

6,9441,056

0,6310,3740,0020,0082,7921,1730,019-

1,4470,5532,000

0,5420,0440,586

15,586

2

ed

Bk 7267.8.92

50,380,097,220,022,579,100,2013,789,260,223,150,17

2,0698,22

7,3290,671

0,5670,2810,0020,0072,9881,1070,0250,024

1,4430,5572,000

0,3320,0320,364

15,364

2

ac-hbl

Bk 7457.8.92

47,590,048,160,014,146,900,1715,0911,000,182,590,15

2,0598,06

6,9601,040

0,3670,4550,0010,0033,2900,8440,0210,019

1,7240,2762,000

0,4580,0290,487

15,487

2

mag-hbl

Bk 7527.8.92

52,270,043,860,062,286,820,1917,3411,790,251,520,09

2,0998,60

7,5090,491

0,1620,2470,0070,0033,7130,8190,0230,027

1,8150,1852,000

0,2380,0170,255

15,255

2

act

Bk 82329.1.93b

48,780,1611,610,011,4211,440,1111,078,230,164,030,29

2,0799,39

7,0530,947

1,0320,1540,0010,0122,3861,3840,0130,017

1,2750,7252,000

0,4050,0550,459

15,459

2

barr

Bk 82429.1.93b

48,090,149,260,014,288,880,0613,219,850,203,040,31

2,0799,40

6,9761,024

0,5590,4670,0010,0112,8561,0770,0070,021

1,5310,4692,000

0,3860,0590,444

15,444

2

mag-hbl

Bk 982.7.94

50,670,056,520,003,716,390,0716,1911,370,251,740,17

2,1099,23

7,2460,754

0,3450,4000,0000,0053,4510,7640,0080,026

1,7420,2582,000

0,2250,0320,256

15,256

2

mag-hbl

Bk 992.7.94

48,960,039,950,003,537,980,0913,409,590,132,890,19

2,0898,82

7,0570,943

0,7480,3830,0000,0032,8790,9620,0110,014

1,4810,5192,000

0,2890,0360,324

15,324

2

mag-hbl

Bk 9523.2.94

47,330,058,220,042,0610,580,1313,3511,760,161,690,23

2,0297,62

7,0230,977

0,4610,2300,0050,0062,9531,3120,0160,018

1,8700,1302,000

0,3560,0440,400

15,400

2

mag-hbl

Bk 10 B2018.10.93

49,600,058,460,004,799,350,1712,749,930,372,410,26

2,09100,22

7,1310,869

0,5640,5180,0000,0042,7301,1240,0210,039

1,5300,4702,000

0,2010,0490,250

15,250

2

mag-hbl

Bk 10 B2118.10.93

50,500,108,080,004,948,330,0913,189,580,162,180,22

2,0999,45

7,2460,754

0,6120,5340,0000,0082,8191,0000,0110,017

1,4730,5272,000

0,0790,0410,120

15,120

2

mag-hbl

Bk 10 B519.10.93b

46,960,547,940,018,6313,180,268,418,600,212,450,29

2,0199,49

7,0130,987

0,4110,9700,0010,0431,8721,6460,0330,023

1,3760,6242,000

0,0860,0560,142

15,142

2

mag-hbl

Bk 10 B719.10.93b

46,550,177,370,028,5213,270,268,809,190,272,280,30

1,9998,99

7,0050,995

0,3130,9640,0020,0141,9741,6700,0330,030

1,4820,5182,000

0,1470,0590,206

15,206

2

mag-hbl

Bk 18135.8.94

49,310,195,050,009,5610,410,5110,878,940,202,100,18

2,0399,35

7,2770,723

0,1561,0620,0000,0212,3911,2850,0640,022

1,4140,5862,000

0,0150,0350,049

15,049

2

ac-hbl

Bk 1826.8.94

52,000,198,530,002,759,000,1412,417,490,203,440,14

2,0998,37

7,4650,535

0,9090,2970,0000,0212,6561,0800,0170,021

1,1520,8482,000

0,1100,0260,136

15,136

2

barr

Bk 1856.8.94

49,180,135,060,017,8012,600,4110,569,850,151,780,16

2,0399,72

7,2770,723

0,1600,8680,0010,0142,3291,5600,0510,016

1,5620,4382,000

0,0720,0310,103

15,103

2

ac-hbl

Bk 1866.8.94

48,840,215,770,009,7211,430,369,978,300,182,670,20

2,0399,67

7,2180,782

0,2231,0800,0000,0232,1961,4120,0450,020

1,3140,6862,000

0,0790,0390,118

15,118

2

barr

Bk 1876.8.94

48,970,205,780,0310,0211,400,409,978,520,272,520,22

2,04100,34

7,1990,801

0,2001,1090,0030,0222,1851,4020,0500,029

1,3420,6582,000

0,0600,0420,102

15,102

2

mag-hbl

Bk 1886.8.94

51,250,158,460,034,359,050,1411,917,300,053,520,13

2,0898,42

7,3940,606

0,8320,4730,0030,0162,5611,0920,0170,005

1,1280,8722,000

0,1130,0240,137

15,137

2

barr

Bk 392624.6.92

45,400,2410,750,035,4011,640,1510,038,25n.a.4,170,32

2,0198,39

6,7761,224

0,6670,6070,0040,0192,2311,4530,019-

1,3190,6812,000

0,5260,0620,588

15,588

2

mag-kat

C-48 Appendix C Table C15/C16 amphibole aroundglaucophane/in symplectite

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name

amphibole names after Leake (1978): ac-hbl is actinolitic-hornblende, act is actinolite, barr is barroisite, ed isedenite, ed-hbl is edenitic-hornblende, mag-hbl is magnesio-hornblende, mag-kat is magnesio-katophorite


sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Cig 91-17817.6.93

45,400,2611,950,002,0211,210,1311,9610,710,093,120,39

2,0499,28

6,6671,333

0,7350,2230,0000,0212,6181,3770,0160,010

1,6850,3152,000

0,5730,0750,648

15,648

2

ed-hbl

Cig 91-13116.6.93

48,180,1214,000,024,1211,100,078,895,850,005,190,35

2,0999,98

6,9241,076

1,2960,4460,0020,0091,9041,3340,0090,000

0,9011,0992,000

0,3470,0660,413

15,413

2

barr

Cig 91-17617.6.93

52,190,1410,820,011,808,990,0812,025,830,045,160,20

2,1299,40

7,3820,618

1,1850,1920,0010,0112,5341,0630,0100,004

0,8831,1172,000

0,2990,0370,335

15,335

2

barr

Cig 91-17717.6.93

54,360,0712,010,010,9910,410,059,842,940,006,460,09

2,1499,37

7,6220,378

1,6060,1040,0010,0052,0561,2210,0060,000

0,4421,5582,000

0,1980,0160,214

15,214

2

gln

Bk 10 B1619.10.93

51,550,086,840,051,758,690,0414,7110,610,151,770,17

2,0898,49

7,4180,582

0,5780,1890,0060,0063,1551,0450,0050,016

1,6360,3642,000

0,1300,0320,161

15,161

2

act-hbl

Bk 10 B1 q18.10.93

54,790,031,790,082,899,080,1416,4212,010,350,610,03

2,11100,33

7,7760,224

0,0750,3090,0090,0023,4731,0770,0170,037

1,8260,1681,994

0,0000,0060,006

15,006

2

act

Bk 10 B8 q18.10.93

55,510,031,620,000,899,840,1216,8312,060,190,750,07

2,11100,02

7,8730,127

0,1440,0950,0000,0023,5581,1670,0140,020

1,8330,1672,000

0,0390,0130,052

15,052

2

act

Bk 10 B9 q18.10.93

52,290,085,180,032,959,170,1614,7510,750,181,620,15

2,0999,39

7,5030,497

0,3790,3180,0030,0063,1551,1000,0190,019

1,6530,3472,000

0,1030,0280,131

15,131

2

act

Bk 10 B10 q18.10.93

55,600,041,670,201,609,220,1516,9412,010,160,720,06

2,13100,50

7,8430,157

0,1210,1690,0220,0033,5621,0880,0180,017

1,8150,1852,000

0,0120,0110,023

15,023

2

act

Bk 10 B11 q18.10.93

54,220,073,630,003,078,900,1315,5010,860,351,360,12

2,12100,32

7,6820,318

0,2880,3270,0000,0053,2731,0540,0160,037

1,6480,3522,000

0,0220,0220,044

15,044

2

act

Bk 10 B12 q18.10.93

53,640,104,170,002,678,770,2015,5111,020,001,170,13

2,1099,48

7,6430,357

0,3430,2860,0000,0083,2941,0450,0240,000

1,6820,3182,000

0,0060,0240,030

15,030

2

act

Bk 10 B1618.10.93

51,720,026,180,023,378,160,1215,3010,930,201,930,17

2,11100,23

7,3530,647

0,3880,3600,0020,0023,2420,9700,0140,021

1,6650,3352,000

0,1970,0310,228

15,228

2

act-hbl

Bk 10 B1718.10.93

53,180,025,120,004,997,261,1515,2211,010,261,530,15

2,14102,03

7,4420,558

0,2860,5260,0000,0023,1740,8490,1360,027

1,6510,3492,000

0,0660,0270,093

15,093

2

act-hbl

Bk 10 B31 q18.10.93

54,410,093,530,180,648,930,0716,7811,940,060,950,11

2,1299,81

7,7030,297

0,2920,0690,0200,0073,5411,0570,0080,006

1,8110,1892,000

0,0720,0200,092

15,092

2

act

Bk 10 B32 q18.10.93

54,560,113,530,110,869,850,1016,0311,440,311,380,12

2,12100,53

7,7130,287

0,3010,0920,0120,0083,3781,1650,0120,032

1,7330,2672,000

0,1110,0220,133

15,133

2

act

C-49Appendix C Table C16 amphiboleinsymplectite

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name

analysis q is in contact with quartz, amphibole names after Leake (1978): ac-hbl is actinolitic-hornblende, act isactinolite, barr is barroisite, ed is edenite, ed-hbl is edenitic-hornblende, mag-hbl is magnesio-hornblende


sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Bk 10 B35 q18.10.93

55,660,093,110,200,109,470,1216,5411,240,021,270,10

2,13100,05

7,8400,160

0,3560,0110,0220,0073,4721,1150,0140,002

1,6960,3042,000

0,0430,0180,061

15,061

2

act

Bk 10 B39 q18.10.93

53,500,114,690,222,418,230,1416,0211,210,201,460,16

2,12100,48

7,5510,449

0,3320,2560,0250,0083,3700,9710,0170,021

1,6950,3052,000

0,0950,0290,124

15,124

2

act

Bk 10 B4218.10.93

51,840,096,040,063,507,070,0915,7510,860,101,680,19

2,1099,37

7,3870,613

0,4020,3750,0070,0073,3450,8430,0110,011

1,6580,3422,000

0,1220,0350,158

15,158

2

act-hbl

Bk 10 B10 q26.11.93

54,850,031,340,001,819,200,0816,9312,240,380,560,11

2,1099,63

7,8280,172

0,0540,1940,0000,0023,6021,0980,0100,040

1,8720,1282,000

0,0270,0200,047

15,047

2

act

Bk 10 B11 q26.11.93

54,290,051,880,062,428,990,1216,3811,740,300,770,08

2,0999,17

7,7850,215

0,1030,2620,0070,0043,5011,0780,0150,032

1,8040,1962,000

0,0180,0150,033

15,033

2

act

Bk 10 B1226.11.93

51,710,135,870,043,838,250,1014,7410,630,181,620,17

2,0999,36

7,4120,588

0,4040,4130,0050,0103,1490,9890,0120,019

1,6330,3672,000

0,0830,0320,115

15,115

2

act-hbl

Bk 10 B1326.11.93

49,990,146,830,024,488,560,2013,9310,650,161,730,21

2,0798,97

7,2440,756

0,4110,4880,0020,0113,0091,0370,0250,017

1,6540,3462,000

0,1400,0400,179

15,179

2

mag-hbl

Bk 1727 q25.7.94

51,720,114,230,043,1410,410,1814,2810,890,011,500,16

2,0698,74

7,5260,474

0,2520,3440,0050,0123,0971,2670,0220,001

1,6980,3022,000

0,1210,0300,151

15,151

2

act

Bk 1728 q25.7.94

52,210,093,780,023,6010,370,2014,3010,950,001,290,13

2,0799,01

7,5740,426

0,2200,3930,0020,0103,0921,2580,0250,000

1,7020,2982,000

0,0650,0250,089

15,089

2

act

Bk 172925.7.94

52,440,073,890,014,0410,350,2714,0810,630,021,500,13

2,0899,50

7,5740,426

0,2360,4390,0010,0083,0311,2500,0330,002

1,6450,3552,000

0,0650,0240,090

15,090

2

act

Bk 17523.7.94

47,420,2110,630,014,379,750,1311,559,030,063,140,30

2,0598,65

6,9321,068

0,7640,4800,0010,0232,5171,1920,0160,006

1,4140,5862,000

0,3040,0570,362

15,362

2

mag-hbl

Bk 17533.7.94

47,180,2010,350,014,369,610,1411,969,250,003,210,32

2,0598,63

6,9071,093

0,6930,4800,0010,0222,6101,1760,0170,000

1,4510,5492,000

0,3620,0610,423

15,423

2

mag-hbl

Bk 17543.7.94

48,700,167,680,035,949,770,3012,319,720,002,470,26

2,0699,40

7,1020,898

0,4220,6520,0030,0182,6761,1920,0370,000

1,5190,4812,000

0,2170,0490,267

15,267

2

mag-hbl

Bk 17553.7.94

46,870,259,160,046,0710,130,3211,019,170,122,750,33

2,0298,25

6,9481,052

0,5480,6770,0050,0282,4331,2560,0400,013

1,4560,5442,000

0,2470,0640,310

15,310

2

mag-hbl

Bk 1749.7.94

54,170,072,850,033,379,560,2415,0510,490,071,440,07

2,0999,50

7,7540,246

0,2350,3630,0030,0083,2111,1440,0290,007

1,6090,3912,000

0,0080,0130,021

15,021

2

act

Bk 1769.7.94

51,880,125,410,035,088,890,2913,629,560,122,080,14

2,0899,30

7,4720,528

0,3900,5510,0030,0132,9241,0710,0350,013

1,4750,5252,000

0,0560,0260,082

15,082

2

act-hbl

Bk 177 q9.7.94

53,510,062,500,032,3810,850,2614,6810,970,061,160,09

2,0798,61

7,7690,231

0,1970,2600,0030,0073,1771,3170,0320,006

1,7070,2932,000

0,0330,0170,050

15,050

2

act

Bk 178 q9.7.94

51,770,124,020,055,2711,100,2112,9510,000,081,790,17

2,0699,60

7,5250,475

0,2140,5770,0060,0132,8061,3500,0260,009

1,5570,4432,000

0,0620,0320,094

15,094

2

act

Bk 17109.7.94

50,820,156,730,155,299,050,2112,969,150,002,470,16

2,0899,22

7,3380,662

0,4840,5750,0170,0162,7891,0930,0260,000

1,4160,5842,000

0,1070,0300,137

15,137

2

act-hbl

Bk 17429.7.94

46,450,2510,090,056,1811,220,1510,429,300,032,850,39

2,0499,42

6,8401,160

0,5910,6850,0060,0282,2871,3820,0190,003

1,4670,5332,000

0,2810,0750,356

15,356

2

mag-hbl

Bk 17509.7.94

50,600,146,680,034,3110,420,4412,539,390,002,550,19

2,0799,35

7,3410,659

0,4830,4700,0030,0152,7091,2650,0540,000

1,4600,5402,000

0,1770,0360,213

15,213

2

act-hbl

Bk 17519.7.94

50,270,167,380,024,879,390,3212,899,460,032,560,20

2,0899,63

7,2510,749

0,5060,5290,0020,0172,7711,1320,0390,003

1,4620,5382,000

0,1780,0380,216

15,216

2

act-hbl

C-50 Appendix C Table C16 amphibole insymplectite

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name



sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Bk 1850 q25.7.94

52,360,034,470,071,318,850,1616,1011,820,221,290,12

2,0898,89

7,5310,469

0,2880,1420,0080,0033,4511,0650,0190,023

1,8210,1792,000

0,1810,0220,204

15,204

2

act

Bk 185125.7.94

50,250,075,450,023,868,390,2314,8711,330,301,480,15

2,0698,46

7,3200,680

0,2560,4230,0020,0083,2291,0220,0280,032

1,7680,2322,000

0,1860,0280,215

15,215

2

act-hbl

Bk 185325.7.94

51,680,065,440,074,007,980,2014,8310,390,211,820,16

2,0898,92

7,4400,560

0,3630,4340,0080,0063,1820,9600,0240,022

1,6030,3972,000

0,1110,0300,141

15,141

2

act-hbl

Bk 18145.8.94

49,650,138,990,113,428,790,1312,778,970,212,940,20

2,0798,38

7,1990,801

0,7360,3730,0130,0142,7601,0660,0160,022

1,3940,6062,000

0,2200,0380,258

15,258

2

mag-hbl

Bk 18155.8.94

52,580,096,060,086,044,690,1015,859,510,232,190,13

2,1399,67

7,4140,586

0,4210,6410,0090,0103,3310,5530,0120,024

1,4370,5632,000

0,0350,0240,059

15,059

2

act-hbl

Bk 1816 q5.8.94

53,160,105,220,052,517,800,1615,4010,130,191,910,11

2,1098,84

7,5880,412

0,4670,2700,0060,0113,2770,9310,0190,020

1,5490,4512,000

0,0780,0200,098

15,098

2

act

Bk 392513.3.93

50,530,176,630,021,088,170,0815,8310,780,112,550,22

2,0798,24

7,3120,688

0,4430,1170,0020,0133,4140,9890,0100,012

1,6710,3292,000

0,3870,0410,428

15,428

2

act-hbl

Bk 392713.3.93

51,450,086,460,023,287,470,1115,5710,250,212,670,18

2,1199,86

7,3260,674

0,4100,3520,0020,0063,3040,8900,0130,022

1,5640,4362,000

0,3010,0330,334

15,334

2

act-hbl

Bk 395224.6.92

49,030,116,990,032,858,680,0914,7610,560,002,680,19

2,0598,01

7,1760,824

0,3810,3140,0030,0093,2201,0620,0110,000

1,6560,3442,000

0,4160,0360,453

15,453

2

mag-hbl

Bk 395324.6.92

49,010,107,840,002,889,060,0813,869,630,003,180,19

2,0597,89

7,1760,824

0,5290,3180,0000,0083,0251,1100,0100,000

1,5110,4892,000

0,4140,0360,450

15,450

2

mag-hbl

Bk 7557.7.92

46,900,1510,550,041,7210,490,1812,079,280,003,580,24

2,0297,22

6,9551,045

0,7990,1920,0050,0122,6681,3020,0230,000

1,4750,5252,000

0,5040,0460,550

15,550

2

edenite

Bk 7437.8.92

46,570,069,650,033,0510,180,1912,4410,010,203,220,21

2,0297,84

•

6,9061,094

0,5930,3410,0040,0052,7501,2630,0240,022

1,5900,4102,000

0,5160,0410,557

15,557

2

edenite

Bk 7477.8.92

47,260,049,510,003,379,640,2112,8610,100,153,100,20

2,0498,48

6,9391,061

0,5840,3720,0000,0032,8141,1840,0260,016

1,5890,4112,000

0,4710,0380,510

15,510

2

edenite

Bk 8514.3.93

49,980,158,950,083,048,070,1213,809,200,163,190,24

2,0999,07

7,1790,821

0,6950,3290,0090,0122,9550,9700,0150,017

1,4160,5842,000

0,3040,0450,349

15,349

2

mag-hbl

Bk 81714.3.93

51,230,036,460,000,628,830,1115,5310,700,192,520,16

2,0898,45

7,3930,607

0,4920,0670,0000,0023,3401,0650,0130,020

1,6540,3462,000

0,3590,0300,390

15,390

2

act-hbl

Bk 81814.3.93

48,240,0510,670,002,868,180,1013,269,370,233,380,26

2,0798,67

6,9801,020

0,7990,3110,0000,0042,8600,9890,0120,025

1,4530,5472,000

0,4010,0490,450

15,450

2

mag-hbl

Bk 856 q14.3.93

54,680,031,130,022,348,490,0617,0211,440,181,070,06

2,0998,61

7,8580,142

0,0490,2530,0020,0023,6461,0200,0070,019

1,7610,2392,000

0,0600,0110,071

15,071

2

act

Bk 857 q14.3.93

54,970,000,560,000,9310,240,0416,6311,870,230,780,03

2,0798,36

7,9500,050

0,0460,1010,0000,0003,5851,2390,0050,025

1,8390,1612,000

0,0580,0060,064

15,064

2

act

Bk 82 q29.1.93b

53,110,083,430,060,709,700,0615,5710,730,181,700,10

2,0697,48

7,7340,266

0,3230,0770,0070,0063,3791,1810,0070,019

1,6740,3262,000

0,1540,0190,173

15,173

2

act

Bk 834 q29.1.93b

54,380,041,500,043,228,400,0416,4911,100,261,180,05

2,0998,79

7,8150,185

0,0690,3480,0050,0033,5321,0100,0050,028

1,7090,2912,000

0,0380,0090,047

15,047

2

act

Bk 9212.7.94

50,130,047,850,070,498,260,1515,4811,650,141,680,24

2,0898,26

7,2370,763

0,5730,0540,0080,0043,3310,9970,0180,015

1,8020,1982,000

0,2720,0450,317

15,317

2

mag-hbl

Bk 9222.7.94

50,370,028,620,040,028,990,0914,7111,270,211,780,22

2,0898,41

7,2550,745

0,7180,0020,0050,0023,1581,0820,0110,022

1,7390,2612,000

0,2360,0410,278

15,278

2

act-hbl

C-51Appendix C Table C16/C17 amphiboleinsymplectite/titanite

sampleanalysisdate

SiO2TiO2Al2O3Fe2O3CaO

total

FH2O

Si

TiAlFe3

Casum

FOH

Bk 10B719.10.93a

30,7536,672,030,4728,90

98,82

0,510,32

1,002

0,8990,0780,011

1,0093,000

0,0530,037

Bk 10B819.10.93a

29,8938,481,380,3028,60

98,65

0,000,52

0,982

0,9510,0530,007

1,0073,000

0,0000,061

Bk 10B919.10.93a

30,0237,341,980,3129,09

98,74

0,010,72

0,981

0,9170,0760,008

1,0183,000

0,0010,083

Bk 10B1019.10.93a

30,4237,151,990,2728,80

98,63

0,000,72

0,995

0,9130,0770,007

1,0093,000

0,0000,083

Bk 17463.7.94

30,1937,791,420,4728,60

98,47

0,270,33

0,992

0,9340,0550,012

1,0073,000

0,0280,038

Bk 17449.7.94

30,5336,252,640,6628,83

98,91

0,330,72

0,992

0,8860,1010,016

1,0043,000

0,0340,083

Bk 396728.1.93

29,9837,411,760,5228,77

98,44

0,530,24

0,984

0,9230,0680,013

1,0123,000

0,0550,026

Bk 391628.7.92

29,7037,781,450,4328,75

98,11

0,370,26

0,980

0,9370,0560,011

1,0163,000

0,0390,029

Bk 392728.7.92

30,2037,032,050,2029,29

98,77

0,790,02

0,985

0,9080,0790,005

1,0233,000

0,0810,002

Bk 39143.7.94

30,3037,551,680,3128,64

98,48

0,120,52

0,994

0,9260,0650,008

1,0073,000

0,0120,060

Bk 39153.7.94

30,4037,081,560,2728,80

98,11

0,250,35

1,000

0,9170,0600,007

1,0153,000

0,0260,041

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name



Bk 96 q23.2.94

52,040,124,990,040,859,160,0515,6211,430,191,390,13

2,0798,09

7,5330,467

0,3840,0930,0050,0133,3701,1090,0060,020

1,7730,2272,000

0,1630,0250,187

15,187

2

act

Bk 9823.2.94

51,450,086,810,001,968,120,1114,7410,050,142,150,14

2,0797,82

7,4350,565

0,5940,2130,0000,0093,1750,9810,0130,015

1,5560,4442,000

0,1580,0260,185

15,185

2

act-hbl

Bk 912 q23.2.94

53,630,054,350,040,079,290,0816,2511,490,111,420,08

2,1098,95

7,6600,340

0,3920,0070,0050,0053,4601,1090,0100,012

1,7580,2422,000

0,1520,0150,167

15,167

2

act

Bk 91323.2.94

50,360,128,090,031,768,810,1213,9510,030,232,370,18

2,0798,13

7,2930,707

0,6740,1920,0030,0133,0111,0680,0150,025

1,5560,4442,000

0,2220,0340,256

15,256

2

act-hbl

Bk 92724.2.94

49,400,008,100,062,737,980,0514,5610,570,112,310,14

2,0798,07

7,1720,828

0,5580,2980,0070,0003,1510,9690,0060,012

1,6440,3562,000

0,2940,0260,321

15,321

2

mag-hbl

Bk 92924.2.94

49,440,148,460,001,699,600,0713,459,990,122,540,21

2,0597,76

7,2210,779

0,6770,1860,0000,0152,9281,1720,0090,013

1,5630,4372,000

0,2820,0400,322

15,322

2

mag-hbl

Bk 9224.3.94

48,770,149,260,053,6810,300,1512,309,960,202,600,25

2,0799,73

7,0590,941

0,6380,4010,0060,0152,6541,2470,0180,021

1,5450,4552,000

0,2740,0470,321

15,321

2

mag-hbl

Bk 9234.3.94

48,770,178,580,002,8310,590,1512,6710,270,162,450,25

2,0698,95

7,1130,887

0,5880,3110,0000,0192,7541,2920,0190,017

1,6050,3952,000

0,2980,0480,345

15,345

2

mag-hbl

Cig 91-17317.6.93

47,670,288,820,000,989,380,0915,0511,680,002,660,33

2,0699,00

6,9391,061

0,4530,1080,0000,0223,2651,1410,0110,000

1,8220,1782,000

0,5720,0630,635

15,635

2

edenite

Cig 91-17417.6.93

45,180,2612,610,021,6310,110,1212,4010,240,003,550,40

2,0498,55

6,6401,360

0,8240,1800,0020,0212,7161,2420,0150,000

1,6120,3882,000

0,6240,0770,701

15,701

2

ed-hbl

normed on 3 kations

C-52 Appendix C Table C17 titanite

sampleanalysisdate


total

FH2O

Si

TiAlFe3

Casum

FOH

normed on 3 kations

sampleanalysisdate


total

FH2O

Si

TiAlFe3

Casum

FOH

normed on 3 kations

sampleanalysisdate


total

FH2O

Si

TiAlFe3

Casum

FOH

normed on 3 kations

Bk 39163.7.94

30,3938,441,180,3628,61

98,98

0,230,26

0,995

0,9470,0460,009

1,0043,000

0,0240,030

Bk 39173.7.94

30,3937,641,530,3228,80

98,68

0,270,34

0,995

0,9270,0590,008

1,0113,000

0,0280,039

Bk 39183.7.94

30,2637,831,130,3928,85

98,46

0,020,44

0,995

0,9350,0440,010

1,0163,000

0,0020,051

Bk 39193.7.94

30,2938,731,020,4028,50

98,94

0,010,42

0,994

0,9550,0390,010

1,0023,000

0,0010,048

Bk 39293.7.94

30,3838,161,300,3028,75

98,89

0,010,49

0,995

0,9390,0500,007

1,0083,000

0,0010,057

Bk 39303.7.94

30,4238,461,080,2828,82

99,06

0,000,42

0,995

0,9460,0420,007

1,0103,000

0,0000,048

Bk 39323.7.94

30,5138,511,010,3228,67

99,02

0,000,41

0,999

0,9480,0390,008

1,0063,000

0,0000,047

Bk 39333.7.94

30,4037,911,390,3928,55

98,64

0,000,55

0,997

0,9350,0540,010

1,0043,000

0,0000,063

Bk 39373.7.94

30,2737,161,870,5828,52

98,40

0,200,57

0,993

0,9170,0720,014

1,0033,000

0,0210,066

Bk 39383.7.94

30,4938,701,040,3828,40

99,01

0,140,30

0,999

0,9540,0400,009

0,9973,000

0,0150,035

Bk 39393.7.94

30,3237,811,400,3828,75

98,66

0,360,23

0,994

0,9320,0540,009

1,0103,000

0,0370,026

Bk 396628.1.93

29,1337,161,460,4828,57

96,80

0,000,62

0,974

0,9340,0580,012

1,0233,000

0,0000,070

Bk 39403.7.94

30,1438,041,160,3928,67

98,40

0,110,37

0,992

0,9420,0450,010

1,0113,000

0,0110,043

Bk 3910,25.5.92

29,4938,400,800,3228,56

97,57

0,020,34

0,981

0,9610,0310,008

1,0183,000

0,0020,037

Bk 3911,25.5.92

30,1636,751,630,5028,84

97,88

0,270,43

0,994

0,9110,0630,012

1,0193,000

0,0280,048

Bk 7462.7.94

29,8037,351,780,3628,78

98,07

0,260,44

0,981

0,9250,0690,009

1,0163,000

0,0270,051

Bk 7472.7.94

30,1436,352,430,2728,54

97,73

0,260,63

0,992

0,9000,0940,007

1,0073,000

0,0270,074

Bk 7482.7.94

30,2438,051,430,1828,99

98,89

0,210,33

0,989

0,9360,0550,004

1,0163,000

0,0220,038

Bk 7492.7.94

30,3438,301,050,3028,76

98,75

0,150,28

0,996

0,9450,0410,007

1,0113,000

0,0160,032

Bk 7512.7.94

30,2137,771,700,2228,71

98,61

0,290,35

0,990

0,9310,0660,005

1,0083,000

0,0300,041

Bk 7187.7.92

29,7535,942,510,2029,07

97,47

0,650,32

0,980

0,8910,0970,005

1,0263,000

0,0680,035

Bk 4127.6.94

30,2637,211,930,2229,02

98,64

0,180,53

0,989

0,9150,0740,005

1,0163,000

0,0190,061

Bk 4227.6.94

30,3637,221,950,2229,03

98,78

0,060,64

0,991

0,9140,0750,005

1,0153,000

0,0060,074

Bk 4327.6.94

30,4737,282,100,1728,92

98,94

0,170,58

0,993

0,9130,0810,004

1,0093,000

0,0180,067

Bk 4427.6.94

30,4837,422,000,2728,98

99,15

0,230,52

0,991

0,9150,0770,007

1,0103,000

0,0240,060

Bk 4527.6.94

30,0736,652,030,1828,95

97,88

0,090,67

0,989

0,9070,0790,004

1,0213,000

0,0090,074

Bk 4627.6.94

30,2937,281,980,2428,91

98,70

0,120,60

0,990

0,9160,0760,006

1,0123,000

0,0120,070

Bk 4727.6.94

30,4637,442,060,2029,06

99,22

0,060,72

0,990

0,9150,0790,005

1,0123,000

0,0060,078

Bk 4827.6.94

30,6437,361,930,2629,03

99,22

0,130,62

0,996

0,9130,0740,006

1,0113,000

0,0130,067

Bk 4927.6.94

30,2938,271,440,2128,97

99,18

0,270,30

0,988

0,9390,0550,005

1,0133,000

0,0280,033

Bk 41027.6.94

30,4937,282,120,1729,01

99,07

0,000,79

0,992

0,9120,0810,004

1,0113,000

0,0000,085

Bk 41127.6.94

30,3737,871,660,1728,90

98,97

0,340,30

0,991

0,9300,0640,004

1,0113,000

0,0350,033

Bk 4649.7.94

30,3339,910,180,4228,91

99,75

0,110,05

0,991

0,9800,0070,010

1,0123,000

0,0110,006

C-53Appendix C Table C17/C18/C19 titanite/ilmenite/dark mica

sampleanalysisdate


total

FH2O

Si

TiAlFe3

Casum

FOH

normed on 3 kations

Bk 942.7.94

30,0637,671,690,2628,59

98,27

0,090,54

0,989

0,9320,0660,006

1,0083,000

0,0090,062

Bk 952.7.94

30,0736,902,000,2628,91

98,14

0,230,52

0,988

0,9110,0770,006

1,0173,000

0,0240,060

Bk 9122.7.94

30,1538,211,390,3428,42

98,51

0,160,39

0,991

0,9450,0540,009

1,0013,000

0,0170,046

Bk 9132.7.94

29,4136,851,580,2829,47

97,59

0,350,27

0,972

0,9160,0620,007

1,0443,000

0,0370,032

Bk 9142.7.94

30,3137,371,700,3128,83

98,52

0,410,27

0,993

0,9210,0660,008

1,0123,000

0,0420,031

Bk 9152.7.94

30,2438,111,480,2128,56

98,60

0,360,22

0,993

0,9410,0570,005

1,0043,000

0,0370,025

sampleanalysisdate

SiO2TiO2Al2O3FeOMnOMgONa2OK2O

FH2Ototal

SiAlt

AloTi

FeMgMn

NaK

sum

FOH

Mg/(Mg+Fe)

Cig 91-14117.6.93

34,560,4719,7216,850,0712,130,529,79

0,191,8794,11

2,6471,3383,985

0,4420,0190,461

1,0791,3850,0052,469

0,0770,9771,055

7,970

0,0921,908

0,562

Cig 91-18116.6.93

34,700,1720,7717,480,1311,020,679,05

0,001,9693,99

2,6511,3373,988

0,5330,0070,540

1,1171,2550,0082,380

0,0990,9011,000

7,908

0,0002,000

0,529

Cig 91-18016.6.93

33,690,5120,1018,520,1410,840,598,85

0,341,7793,24

2,6181,3463,963

0,4950,0210,516

1,2031,2550,0092,468

0,0890,8960,985

7,933

0,1671,833

0,511

Cig 91-17916.6.93

33,710,5019,4218,770,0710,920,498,40

0,271,7892,28

2,6441,3393,983

0,4560,0210,477

1,2311,2760,0052,512

0,0750,8590,933

7,904

0,1341,866

0,509

Cig 91-17616.6.93

35,780,3718,6419,100,109,910,409,33

0,001,9493,63

2,7681,3084,076

0,3910,0150,407

1,2361,1430,0072,385

0,0600,9411,001

7,868

0,0002,000

0,480

Cig 91-17516.6.93

34,060,0620,0519,500,169,480,389,70

0,001,9293,39

2,6591,3353,994

0,5100,0030,512

1,2731,1030,0112,387

0,0580,9871,045

7,938

0,0002,000

0,464

Cig 91-17416.6.93

34,300,4919,9319,440,159,920,399,69

0,001,9494,31

2,6531,3373,990

0,4800,0200,500

1,2571,1440,0102,411

0,0580,9771,035

7,936

0,0002,000

0,476

Cig 91-17316.6.93

34,450,3920,6119,720,0910,120,459,54

0,001,9695,37

2,6311,3423,973

0,5120,0160,528

1,2591,1520,0062,417

0,0670,9491,016

7,934

0,0002,000

0,478

Cig 91-15816.6.93

36,180,0920,2315,750,1312,380,259,62

0,002,0094,63

2,7171,3214,038

0,4700,0040,474

0,9891,3860,0082,383

0,0360,9420,978

7,873

0,0002,000

0,583

Cig 91-15716.6.93

35,610,1319,2018,360,0911,350,289,65

0,061,9494,67

2,7161,3214,037

0,4050,0050,410

1,1711,2900,0062,467

0,0410,9591,001

7,916

0,0291,971

0,524

Cig 91-15116.6.93

34,910,0420,1619,120,1210,270,299,50

0,001,9594,41

2,6781,3304,009

0,4930,0020,494

1,2271,1740,0082,409

0,0430,9500,993

7,905

0,0002,000

0,489

sampledateanalysisposition

TiO2FeOMn

total

Ti

FeMn

Bk 730.6.9452rt

52,0643,881,19

97,13

1,019

0,9550,026

Bk 392.7.9423rt

50,3244,152,04

96,51

0,989

0,9650,045

Bk 392.7.9424grt

50,0244,343,06

97,42

0,973

0,9600,067

Bk 392.7.9426grt

55,2638,375,48

99,11

1,062

0,8200,119

Bk 392.7.9427grt

50,5442,665,06

98,26

0,975

0,9150,110

Bk 392.7.9434rt

53,1144,431,4

98,94

1,020

0,9490,030

Bk 392.7.9436rt

51,5545,21,92

98,67

0,992

0,9670,042

Bk 392.7.9441rt

56,7337,911,79

96,43

1,124

0,8360,040

Bk 392.7.9442rt

51,1444,542,08

97,76

0,993

0,9620,045

normed on 22 oxygens, all Fe assumed Fe2

normed on 2 kations

position: grt is ilmenite in garnet, rt is ilmenite in contact with rutile

C-54 Appendix C Table C20 coarse amphibole

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name

analysis vein is amphibole from a vein, amphibole names after Leake (1978): ac-hbl is actinolitic-hornblende, act isactinolite, barr is barroisite, mag-hbl is magnesio-hornblende


sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Bk 92023.2.94

45,270,1511,040,054,4310,620,1711,0410,020,122,770,28

2,0197,97

6,7391,261

0,6760,4960,0060,0172,4491,3220,0210,013

1,5980,4022,000

0,3970,0540,452

15,452

2

mag-hbl

Bk 91424.2.94

47,260,3010,260,013,2210,050,0912,039,720,072,810,26

2,0498,13

6,9441,056

0,7210,3570,0010,0332,6351,2350,0110,008

1,5300,4702,000

0,3310,0500,380

15,380

2

mag-hbl

Bk 91524.2.94

48,160,289,900,043,229,990,1411,799,040,173,030,23

2,0498,03

7,0610,939

0,7720,3560,0050,0312,5771,2250,0170,018

1,4200,5802,000

0,2820,0440,325

15,325

2

mag-hbl

Bk 91624.2.94

48,380,408,340,103,259,750,1212,9010,250,182,270,23

2,0498,21

7,0950,905

0,5360,3590,0120,0442,8201,1950,0150,019

1,6100,3902,000

0,2560,0440,300

15,300

2

mag-hbl

Bk 92524.2.94

45,990,2210,270,003,4111,110,1411,4610,160,162,780,29

2,0298,01

6,8381,162

0,6370,3810,0000,0252,5401,3820,0180,018

1,6190,3812,000

0,4200,0560,476

15,476

2

mag-hbl

Bk 92624.2.94

46,740,049,890,023,3010,470,1112,0410,180,102,680,28

2,0297,88

6,9211,079

0,6470,3670,0020,0042,6571,2970,0140,011

1,6150,3852,000

0,3840,0540,438

15,438

2

mag-hbl

Bk 10 B3318.10.93

52,090,075,490,003,326,710,0016,1210,820,701,930,17

2,1099,52

7,4200,580

0,3420,3560,0000,0073,4230,7990,0000,074

1,6510,3492,000

0,1840,0320,216

15,216

2

act-hbl

Bk 10 B3418.10.93

53,010,115,000,010,918,830,0015,9711,180,071,530,14

2,1098,86

7,5800,420

0,4220,0980,0010,0123,4041,0560,0000,007

1,7130,2872,000

0,1370,0260,163

15,163

2

act

Bk 10 B4918.10.93

49,790,106,990,003,308,730,0014,5311,060,001,660,30

2,0798,53

7,2280,772

0,4240,3610,0000,0113,1441,0600,0000,000

1,7200,2802,000

0,1880,0570,244

15,244

2

mag-hbl

Bk 10 B5018.10.93

52,180,105,460,004,377,090,1115,7210,970,251,510,22

2,11100,10

7,4040,596

0,3170,4670,0000,0113,3250,8420,0130,026

1,6680,3322,000

0,0830,0410,124

15,124

2

act-hbl

Bk 10 B5218.10.93

50,370,086,490,004,618,980,1014,1811,080,251,580,30

2,09100,11

7,2380,762

0,3370,4990,0000,0093,0371,0790,0120,027

1,7060,2942,000

0,1460,0560,202

15,202

2

mag-hbl

Bk 10 B5418.10.93

50,520,036,700,044,807,470,1314,6510,820,501,710,25

2,0999,71

7,2450,755

0,3780,5180,0050,0033,1320,8960,0160,053

1,6630,3372,000

0,1380,0470,185

15,185

2

mag-hbl

Bk 10 B5518.10.93

50,260,057,060,092,729,240,0814,5511,180,351,970,29

2,0999,92

7,2220,778

0,4180,2940,0100,0053,1161,1100,0100,037

1,7210,2792,000

0,2700,0540,324

15,324

2

mag-hbl

Bk 10 B219.10.93a

47,240,029,240,006,937,110,0013,5710,780,001,830,37

2,0799,16

6,8591,141

0,4400,7580,0000,0022,9370,8640,0000,000

1,6770,3232,000

0,1920,0700,262

15,262

2

mag-hbl

Bk 10 B319.10.93a

50,200,055,580,004,178,030,1515,0611,260,251,500,27

2,0698,58

7,2980,702

0,2540,4560,0000,0053,2630,9760,0180,027

1,7540,2462,000

0,1770,0510,228

15,228

2

act-hbl

Bk 10 B419.10.93a

50,940,065,320,025,706,790,2415,4311,310,301,240,23

2,0999,67

7,3040,696

0,2030,6150,0020,0063,2980,8150,0290,032

1,7380,2622,000

0,0820,0430,125

15,125

2

act-hbl

Bk 185225.7.94

49,570,048,160,064,408,680,2413,159,690,322,580,25

2,0799,21

7,1700,830

0,5610,4790,0070,0042,8351,0500,0290,034

1,5020,4982,000

0,2250,0470,272

15,272

2

mag-hbl

Bk 185525.7.94

52,850,054,970,044,057,930,2314,749,920,241,830,13

2,0999,07

7,5670,433

0,4060,4360,0050,0053,1460,9490,0280,025

1,5220,4782,000

0,0300,0240,054

15,054

2

act

Bk 185625.7.94

51,720,076,720,045,357,710,2913,388,710,262,560,15

2,0999,05

7,4230,577

0,5600,5780,0050,0082,8620,9250,0350,028

1,3390,6612,000

0,0520,0280,080

15,080

2

act-hbl

Bk 185725.7.94

52,960,055,660,032,416,720,1115,839,870,132,090,12

2,1098,08

7,5730,427

0,5270,2590,0030,0053,3740,8040,0130,014

1,5120,4882,000

0,0920,0220,114

15,114

2

act

Bk 185825.7.94

48,730,067,140,063,918,970,2213,7510,880,281,940,18

2,0498,16

7,1520,848

0,3870,4310,0070,0073,0081,1020,0270,030

1,7110,2892,000

0,2630,0340,297

15,297

2

mag-hbl

Bk 1826.8.94

52,000,198,530,002,759,000,1412,417,490,203,440,14

2,0998,37

7,4650,535

0,9090,2970,0000,0212,6561,0800,0170,021

1,1520,8482,000

0,1100,0260,136

15,136

2

barr

C-55Appendix C Table C20/C21 coarseamphibole/chlorite

analysis vein is amphibole from a vein, amphibole names after Leake (1978): ac-hbl is actinolitic-hornblende, act isactinolite, barr is barroisite, mag-hbl is magnesio-hornblende


SiO2TiO2Al2O3Cr2O3Fe2O3FeOMnOMgO

H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)

Bk 10B1427.11.93grt

24,910,0419,880,016,1620,650,1815,25

11,3298,40

5,2782,7228,000

2,2430,0020,0060,9823,6594,8160,03211,741

19,741

16

0,568

Bk 10B1527.11.93grt

25,250,0119,900,006,0720,370,2315,51

11,3898,72

5,3202,6808,000

2,2620,0000,0020,9623,5894,8710,04111,727

19,727

16

0,576

Bk 10B1919.10.93bgrt

25,470,0218,950,045,6921,730,2114,74

11,2498,10

5,4332,5678,000

2,1970,0070,0030,9143,8764,6860,03811,721

19,721

16

0,547

Bk 10B2419.10.93bgrt

24,920,0319,310,046,0021,160,2514,90

11,2297,83

5,3282,6728,000

2,1940,0070,0050,9663,7834,7480,04511,748

19,748

16

0,557

Bk 10B2527.11.93grt

25,220,0820,130,005,6821,390,1814,15

11,2898,11

5,3622,6388,000

2,4070,0000,0130,9093,8034,4840,03211,648

19,648

16

0,541

Bk 10B2627.11.93grt

24,640,0720,250,016,0621,590,2414,06

11,2498,16

5,2572,7438,000

2,3480,0020,0110,9733,8524,4710,04311,699

19,699

16

0,537

Bk 10B2727.11.93grt

24,770,1119,500,025,7622,190,2213,70

11,1397,39

5,3412,6598,000

2,2960,0030,0180,9354,0004,4030,04011,695

19,695

16

0,524

Bk 10B3227.11.93grt

24,790,0520,280,035,8021,590,2213,70

11,2097,66

5,3092,6918,000

2,4270,0050,0080,9353,8664,3730,04011,654

19,654

16

0,531

Bk 10B3327.11.93grt

25,300,1020,040,035,5521,060,1914,21

11,2697,75

5,3902,6108,000

2,4210,0050,0160,8903,7534,5120,03411,631

19,631

16

0,546

Bk 171425.7.94?

26,730,0619,910,015,5518,130,1917,32

11,6699,56

5,4972,5038,000

2,3220,0020,0090,8583,1185,3090,03311,651

19,651

16

0,630

Bk 171525.7.94?

25,840,0519,840,045,9618,010,3717,20

11,5398,85

5,3742,6268,000

2,2380,0070,0080,9343,1335,3320,06511,716

19,716

16

0,630

sampleanalysisdate


H2Ototal

SiAlt

AloFe3CrTiMgFe2MnZn

CaNa

NaK

sum

OH

name


Bk 1836.8.94

47,390,069,770,004,309,730,1212,069,710,182,770,31

2,0498,44

6,9591,041

0,6490,4760,0000,0072,6391,1940,0150,020

1,5280,4722,000

0,3160,0590,376

15,376

2

mag-hbl

Bk 1846.8.94

52,950,054,970,000,1110,580,1514,259,910,182,090,11

2,0697,41

7,7100,290

0,5630,0120,0000,0053,0931,2880,0190,019

1,5460,4542,000

0,1360,0210,157

15,157

2

barr

Bk 1886.8.94

51,250,158,460,034,359,050,1411,917,300,053,520,13

2,0898,42

7,3940,606

0,8320,4730,0030,0162,5611,0920,0170,005

1,1280,8722,000

0,1130,0240,137

15,137

2

act

Bk 1712 vein9.7.94

50,790,113,340,002,1815,280,5011,9311,830,070,880,17

2,0299,11

7,5470,453

0,1320,2440,0000,0122,6421,8990,0630,008

1,8830,1172,000

0,1370,0330,170

15,170

2

act

Bk 1713 vein9.7.94

51,960,082,200,001,7815,520,4912,1311,840,040,540,12

2,0298,72

7,7240,276

0,1090,1990,0000,0092,6881,9290,0620,004

1,8860,1142,000

0,0410,0230,065

15,065

2

act

Bk 1711 vein9.7.94

52,260,082,150,061,2415,820,5312,1911,950,100,560,12

2,0299,08

7,7420,258

0,1170,1380,0070,0092,6921,9590,0670,011

1,8970,1032,000

0,0580,0230,081

15,081

2

act

Bk 1838 vein25.7.94

51,850,163,020,052,6111,300,2414,1711,270,001,070,10

2,0497,88

7,6330,367

0,1570,2890,0060,0183,1091,3910,0300,000

1,7780,2222,000

0,0830,0190,102

15,102

2

act

Bk 1837 vein25.7.94

53,100,062,340,022,039,730,2115,4511,310,050,880,09

2,0597,31

7,7720,228

0,1750,2230,0020,0073,3701,1910,0260,005

1,7740,2262,000

0,0230,0170,040

15,040

2

act

Bk 1836 vein25.7.94

52,080,154,400,002,1512,420,2513,1410,450,001,750,17

2,0699,01

7,5920,408

0,3480,2360,0000,0162,8551,5140,0310,000

1,6320,3682,000

0,1270,0320,159

15,159

2

act

normed on 28 oxygens, Fe3=Al(t)-Al(o)-Cr-2*Ti

position: grt is chlorite at garnet, pg is chlorite at paragonite, v is chlorite in vein, ? is chlorite at undeterminedtextural position

C-56 Appendix C Table C21 chlorite



H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)





H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)


Bk 171625.7.94?

25,600,0619,960,075,7718,050,4116,49

11,4197,83

5,3812,6198,000

2,3260,0120,0090,9133,1745,1670,07311,674

19,674

16

0,619

Bk 171725.7.94?

25,360,0720,400,046,0518,060,3016,63

11,4798,38

5,3032,6978,000

2,3300,0070,0110,9523,1585,1830,05311,693

19,693

16

0,621

Bk 171825.7.94?

25,030,0819,770,035,9819,290,4615,70

11,2997,63

5,3162,6848,000

2,2650,0050,0130,9553,4264,9700,08311,717

19,717

16

0,592

Bk 171925.7.94?

25,390,0920,640,106,1317,810,3216,82

11,5498,84

5,2782,7228,000

2,3360,0160,0140,9593,0975,2120,05611,691

19,691

16

0,627

Bk 172025.7.94?

25,750,1020,000,065,9618,320,4116,86

11,5398,99

5,3572,6438,000

2,2600,0100,0160,9333,1865,2280,07211,705

19,705

16

0,621

Bk 172125.7.94?

25,680,0720,440,035,8017,780,3716,59

11,4998,25

5,3622,6388,000

2,3920,0050,0110,9123,1045,1630,06511,653

19,653

16

0,625

Bk 172225.7.94?

25,900,0519,720,075,7718,170,2816,91

11,4898,36

5,4132,5878,000

2,2700,0120,0080,9083,1765,2670,05011,691

19,691

16

0,624

Bk 172325.7.94?

25,630,0620,330,076,1318,610,3116,75

11,5799,46

5,3132,6878,000

2,2790,0110,0090,9563,2265,1750,05411,711

19,711

16

0,616

Bk 172425.7.94?

25,480,0720,030,056,0118,520,4516,51

11,4698,58

5,3322,6688,000

2,2720,0080,0110,9463,2425,1500,08011,709

19,709

16

0,614

Bk 172525.7.94v

26,510,0519,130,145,5117,190,3217,83

11,5298,21

5,5182,4828,000

2,2100,0230,0080,8642,9925,5310,05611,685

19,685

16

0,649

Bk 172625.7.94v

26,330,1219,250,135,5717,880,3517,34

11,5198,48

5,4852,5158,000

2,2120,0210,0190,8733,1155,3840,06211,686

19,686

16

0,633

Bk 17309.7.94?

25,870,0619,700,005,7518,000,3216,95

11,4698,10

5,4162,5848,000

2,2780,0000,0090,9063,1515,2900,05711,691

19,691

16

0,627

Bk 17319.7.94?

25,890,0819,680,005,7917,710,3617,22

11,4898,21

5,4092,5918,000

2,2560,0000,0130,9113,0945,3630,06411,699

19,699

16

0,634

Bk 17339.7.94?

25,760,0719,930,005,8418,180,3016,82

11,4898,38

5,3832,6178,000

2,2920,0000,0110,9193,1785,2390,05311,692

19,692

16

0,622

Bk 17349.7.94?

26,320,0219,910,005,5817,420,3317,26

11,5498,38

5,4702,5308,000

2,3460,0000,0030,8723,0285,3460,05811,653

19,653

16

0,638

Bk 17359.7.94?

26,070,0919,670,005,7117,060,3017,66

11,5198,07

5,4342,5668,000

2,2650,0000,0140,8962,9735,4860,05311,688

19,688

16

0,649

Bk 17369.7.94?

26,130,0520,060,005,9417,040,3317,92

11,6399,10

5,3902,6108,000

2,2660,0000,0080,9222,9405,5090,05811,703

19,703

16

0,652

Bk 17379.7.94?

26,310,0419,720,005,7416,960,2517,97

11,5898,57

5,4492,5518,000

2,2620,0000,0060,8942,9375,5470,04411,691

19,691

16

0,654

Bk 17704.7.94v

25,910,1119,130,155,9317,260,3218,02

11,5098,33

5,4042,5968,000

2,1070,0250,0170,9313,0115,6020,05711,749

19,749

16

0,650

Bk 17714.7.94v

25,960,0118,980,115,6716,190,2918,21

11,3996,81

5,4672,5338,000

2,1790,0180,0020,8992,8515,7160,05211,717

19,717

16

0,667

Bk 18206.8.94?

25,150,0021,360,005,9915,410,0917,40

11,4696,86

5,2662,7348,000

2,5370,0000,0000,9442,6985,4310,01611,626

19,626

16

0,668

Bk 18216.8.94?

25,580,0220,520,005,7716,470,1017,25

11,4497,15

5,3632,6378,000

2,4340,0000,0030,9112,8875,3910,01811,643

19,643

16

0,651

C-57Appendix C Table C21 chlorite



H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)




H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)



Bk 18226.8.94?

25,130,0121,120,005,9816,360,1316,93

11,4397,09

5,2752,7258,000

2,5000,0000,0020,9452,8725,2970,02311,638

19,638

16

0,648

Bk 9114.3.94?

27,630,0719,480,035,4915,770,1519,69

11,88100,19

5,5782,4228,000

2,2130,0050,0110,8342,6625,9250,02611,675

19,675

16

0,690

Bk 9134.3.94?

26,590,0419,180,005,3716,170,1818,31

11,4997,33

5,5492,4518,000

2,2660,0000,0060,8442,8215,6950,03211,664

19,664

16

0,669

Bk 9164.3.94?

25,310,0420,620,005,8314,370,1418,21

11,3995,92

5,3292,6718,000

2,4450,0000,0060,9242,5305,7140,02511,645

19,645

16

0,693

Bk 9194.3.94?

27,260,0420,240,045,3816,860,1818,06

11,7999,85

5,5452,4558,000

2,3970,0060,0060,8232,8695,4760,03111,608

19,608

16

0,656

Bk 9204.3.94grt

24,610,0721,000,055,9017,970,1715,41

11,2596,43

5,2482,7528,000

2,5250,0080,0110,9463,2054,8980,03111,625

19,625

16

0,604

Bk 9214.3.94grt

25,590,0321,140,045,8917,510,1916,54

11,5498,47

5,3172,6838,000

2,4940,0070,0050,9213,0425,1230,03311,625

19,625

16

0,627

Bk 93724.2.94?

26,100,0319,750,055,5318,220,1916,66

11,4597,99

5,4662,5348,000

2,3410,0080,0050,8723,1915,2010,03411,651

19,651

16

0,620

Bk 93824.2.94?

26,130,0919,580,095,2518,440,2316,12

11,3797,30

5,5142,4868,000

2,3830,0150,0140,8343,2555,0700,04111,613

19,613

16

0,609

Bk 93924.2.94?

25,600,0419,550,105,5917,870,1816,55

11,3196,79

5,4302,5708,000

2,3170,0170,0060,8923,1705,2320,03211,666

19,666

16

0,623

Bk 94024.2.94?

25,820,0519,970,025,8015,160,1418,54

11,4896,98

5,3942,6068,000

2,3120,0030,0080,9122,6495,7730,02511,682

19,682

16

0,685

Bk 94124.2.94?

25,310,0419,930,035,8414,100,1118,73

11,3495,43

5,3552,6458,000

2,3240,0050,0060,9302,4955,9060,02011,687

19,687

16

0,703

Bk 18255.8.94grt

25,490,0720,600,035,7321,670,3414,01

11,4299,36

5,3542,6468,000

2,4540,0050,0110,9063,8074,3860,06011,630

19,630

16

0,535

Bk 18265.8.94grt

25,440,0720,040,015,6221,000,3814,39

11,3298,27

5,3922,6088,000

2,3980,0020,0110,8973,7234,5460,06811,645

19,645

16

0,550

Bk 18275.8.94grt

25,480,0619,880,015,8121,620,3314,55

11,3899,12

5,3722,6288,000

2,3110,0020,0100,9223,8114,5720,05911,687

19,687

16

0,545

Bk 18295.8.94pg

26,250,0021,450,036,0512,340,2520,20

11,8298,39

5,3292,6718,000

2,4610,0050,0000,9252,0956,1120,04311,641

19,641

16

0,745

Bk 18305.8.94pg

26,210,0021,270,095,9812,070,2220,27

11,7797,88

5,3422,6588,000

2,4520,0150,0000,9182,0576,1580,03811,637

19,637

16

0,750

Bk 186325.7.94?

26,150,0320,170,015,8015,710,2218,41

11,5998,09

5,4112,5898,000

2,3290,0020,0050,9032,7185,6780,03911,673

19,673

16

0,676

Bk 186425.7.94?

25,180,0921,240,015,8715,770,2117,06

11,4396,86

5,2822,7188,000

2,5330,0020,0140,9272,7665,3340,03711,614

19,614

16

0,659

Bk 186525.7.94?

25,890,1021,170,045,8816,210,2517,54

11,6598,73

5,3322,6688,000

2,4710,0070,0150,9112,7935,3840,04411,624

19,624

16

0,658

Bk 994.3.94?

26,200,0620,150,005,7816,280,0918,21

11,6198,37

5,4152,5858,000

2,3240,0000,0090,8992,8145,6100,01611,672

19,672

16

0,666

Bk 9104.3.94?

27,480,1620,220,004,9615,970,1418,14

11,7498,82

5,6142,3868,000

2,4820,0000,0250,7632,7295,5230,02411,546

19,546

16

0,669

C-58 Appendix C Table C21 chlorite



H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)




H2Ototal

SiAl t

AloCrTiFe3+Fe2MgMn

OH

Mg/(Mg+Fe2)



Bk 94224.2.94?

25,970,0420,350,015,8014,390,1118,95

11,5697,18

5,3902,6108,000

2,3680,0020,0060,9062,4985,8620,01911,661

19,661

16

0,701

Bk 94324.2.94?

25,390,0520,010,015,8417,420,1916,87

11,3797,15

5,3572,6438,000

2,3330,0020,0080,9273,0745,3050,03411,683

19,683

16

0,633

Bk 94424.2.94?

25,710,0619,180,035,4318,310,2016,32

11,2696,49

5,4792,5218,000

2,2970,0050,0100,8703,2635,1840,03611,665

19,665

16

0,614

Bk 94924.2.94pg

26,040,0421,240,035,9112,420,2219,82

11,6997,41

5,3412,6598,000

2,4760,0050,0060,9122,1306,0600,03811,627

19,627

16

0,740

Bk 95024.2.94pg

26,240,0520,980,065,5712,470,1419,53

11,6296,66

5,4162,5848,000

2,5190,0100,0080,8652,1526,0080,02411,587

19,587

16

0,736

Bk 95324.2.94pg

26,210,0320,520,085,8212,110,1220,39

11,6596,94

5,3952,6058,000

2,3730,0130,0050,9022,0856,2560,02111,654

19,654

16

0,750

Bk 95323.2.94pg

26,210,0020,800,045,7811,270,1320,63

11,6596,51

5,3942,6068,000

2,4400,0070,0000,8951,9406,3290,02311,632

19,632

16

0,765

Bk 95423.2.94pg

26,150,0321,240,026,0910,640,1121,34

11,7997,41

5,3212,6798,000

2,4160,0030,0050,9331,8106,4730,01911,659

19,659

16

0,781

Bk 95424.2.94pg

25,760,0521,500,046,0412,180,1719,82

11,6897,23

5,2902,7108,000

2,4950,0060,0080,9332,0926,0670,03011,630

19,630

16

0,744

Bk 95724.2.94pg

25,780,0121,270,005,9811,480,1520,23

11,6396,53

5,3152,6858,000

2,4840,0000,0020,9271,9806,2170,02611,635

19,635

16

0,758

Bk 95824.2.94pg

25,220,0420,900,116,0011,300,1519,98

11,4595,16

5,2812,7198,000

2,4390,0180,0060,9461,9796,2360,02711,651

19,651

16

0,759

Bk 95924.2.94pg

25,760,0721,660,055,9811,120,1520,26

11,6896,73

5,2902,7108,000

2,5320,0080,0110,9241,9096,2010,02611,612

19,612

16

0,765

Bk 96024.2.94pg

26,310,1121,270,106,0510,890,1021,30

11,8597,97

5,3282,6728,000

2,4040,0160,0170,9221,8446,4290,01711,648

19,648

16

0,777

Bk 96124.2.94pg

26,180,0220,770,065,7611,660,1320,37

11,6496,60

5,3932,6078,000

2,4370,0100,0030,8932,0106,2550,02311,630

19,630

16

0,757

Bk 96224.2.94pg

25,770,0621,450,035,9610,870,0820,50

11,6596,37

5,3052,6958,000

2,5090,0050,0090,9231,8716,2900,01411,620

19,620

16

0,771

Bk 96324.2.94pg

27,010,0919,670,125,2711,310,0921,06

11,6596,26

5,5632,4378,000

2,3380,0200,0140,8161,9496,4650,01611,617

19,617

16

0,768

Bk 96424.2.94pg

26,620,0519,970,135,5311,080,1121,10

11,6496,22

5,4882,5128,000

2,3400,0210,0080,8571,9106,4840,01911,639

19,639

16

0,772

Bk 96524.2.94pg

26,080,0420,950,086,0410,760,1221,23

11,7397,03

5,3332,6678,000

2,3830,0130,0060,9301,8416,4710,02111,664

19,664

16

0,779

Bk 96624.2.94pg

26,120,0922,040,076,1210,230,0821,25

11,8897,88

5,2762,7248,000

2,5220,0110,0140,9311,7286,3970,01411,616

19,616

16

0,787

C-59Appendix C Table C22 epidote

position: grt is epidote in a chlorite, albite, epidote aggregate after garnet, vein is epidote in a vein


SiO2Al2O3Fe2O3CaO

H2Ototal

Si

AlFe3

Ca

OH

X Al2Fe

Bk 17482.7.94grt

37,4024,6311,1523,48

1,8796,66

2,993

2,3230,6712,994

2,013

1

0,68

Bk 17502.7.94grt

37,8525,2910,3123,40

1,8896,85

3,013

2,3730,6182,991

1,996

1

0,62

Bk 17125.7.94grt

37,1423,8113,2023,18

1,8797,33

2,972

2,2460,7953,041

1,987

1

0,76

Bk 17225.7.94grt

37,7524,9611,6023,31

1,8997,62

2,994

2,3330,6923,025

1,981

1

0,68

Bk 17325.7.94grt

37,6724,7811,9223,40

1,8997,77

2,986

2,3150,7113,026

1,987

1

0,69

Bk 17425.7.94grt

37,4224,7611,5523,56

1,8897,29

2,978

2,3220,6913,014

2,009

1

0,68

Bk 17525.7.94grt

37,6724,3412,3123,49

1,8997,81

2,990

2,2770,7353,012

1,998

1

0,73

Bk 17625.7.94grt

37,8325,2711,2823,30

1,8997,68

2,994

2,3580,6723,029

1,976

1

0,65

Bk 17725.7.94grt

37,8126,1710,1823,70

1,9197,86

2,974

2,4260,6033,029

1,997

1

0,59

Bk 17825.7.94grt

37,5624,7011,8923,32

1,8997,47

2,987

2,3150,7123,026

1,987

1

0,69

Bk 17289.7.94grt

36,8624,1211,6923,09

1,8595,76

2,984

2,3010,7123,013

2,003

1

0,70

Bk 17299.7.94grt

37,4823,3413,0822,99

1,8696,89

3,015

2,2130,7923,004

1,981

1

0,79

normed on 8 cations,all Fe assumed Fe3


SiO2Al2O3Fe2O3CaO

H2Ototal

Si

AlFe3

Ca

OH

X Al2Fe

normed on 8 cations,all Fe assumed Fe3

Bk 183125.7.94vein

38,0426,489,1523,16

1,8996,83

3,015

2,4730,5453,019

1,967

1

0,54

Bk 183225.7.94vein

38,0426,509,0123,25

1,8996,80

3,014

2,4750,5373,012

1,974

1

0,53

Bk 183425.7.94vein

37,4826,819,0623,04

1,8896,39

2,981

2,5130,5423,055

1,963

1

0,51

Bk 183525.7.94vein

36,9025,449,7822,77

1,8594,89

2,993

2,4320,5973,029

1,979

1

0,58

Bk 184725.7.94vein

37,6225,8210,0123,17

1,8896,62

2,997

2,4250,6003,025

1,978

1

0,59

Bk 184825.7.94vein

38,0225,939,5723,36

1,8996,88

3,017

2,4250,5712,997

1,986

1

0,57

Bk 184925.7.94vein

37,7425,799,7123,22

1,8896,46

3,009

2,4240,5833,007

1,984

1

0,58

Bk 18205.8.94grt

37,3524,4012,2023,38

1,8897,33

2,978

2,2930,7323,025

1,997

1

0,71

Bk 18215.8.94grt

37,5623,6813,0723,34

1,8897,65

2,995

2,2260,7843,010

1,994

1

0,78

exhumation of ultrahigh-pressure metamorphic oceanic crust

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