m400 final rept final version nov2 2010
TRANSCRIPT
Minerals and Energy Research Institute of Western Australia
Final Report
On-Site Validation and Implementation of New Hylogging Technologies – Technology Transfer and Re-Skilling
M400 Project
Authors: T. J. Roache, J. L. Walshe and J.F. Huntington
iii
TABLE OF CONTENTS
List of Figures .............................................................................................................................. v
Executive Summary .................................................................................................................... vii
Acknowledgements ..................................................................................................................... ix
1 INTRODUCTION ................................................................................................................... 1
1.1 Objective of MERIWA M400 ....................................................................................... 1
1.2 Methodology ............................................................................................................... 1
1.3 Training workshops and on-site instruction ............................................................... 3
2 CLINOZOISITE – EPIDOTE .................................................................................................... 5
2.1 Introduction ................................................................................................................ 5
2.2 Textural & paragenetic interpretation ........................................................................ 5
2.3 Hyperspectral indices and Mineral compositions ....................................................... 7
2.4 Discussion .................................................................................................................... 9
3 AMPHIBOLE ....................................................................................................................... 11
3.1 Introduction .............................................................................................................. 11
3.2 Textural & paragenetic interpretation ...................................................................... 11
3.3 Hyperspectral indices and Mineral compositions ..................................................... 16
3.4 Significance of amphibole - epidote - clinozoisite relations ..................................... 22
4 SPECTRAL MAPPING, VICTORY-DEFIANCE, ST IVES ........................................................... 25
4.1 Geology ..................................................................................................................... 26
4.2 Gold Distribution ....................................................................................................... 27
4.3 Alteration assemblages and assemblage zoning ...................................................... 28
4.4 Paragenetic relations ................................................................................................ 33
4.5 Correlation of spectral characteristics with stable isotopes: constraints on redox
conditions.............................................................................................................................. 34
4.6 Summary ................................................................................................................... 40
5 SPECTRAL AND STABLE ISOTOPE STUDY, WALLABY DEPOSIT, LAVERTON ....................... 41
5.1 Geological Setting ..................................................................................................... 41
5.2 Alteration zoning in the Wallaby Deposit ................................................................. 45
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5.3 Wallaby WB0801CD .................................................................................................. 48
5.4 Stable isotopes, mineral assemblages & spectral characteristics: constraints on
redox conditions .................................................................................................................... 51
5.5 Discussion and Conclusions ....................................................................................... 57
6 BULLANT AU MINE: A 3D MINERAL SYSTEM PERSPECTIVE ............................................... 61
6.1 Introduction............................................................................................................... 61
6.2 Lithology .................................................................................................................... 61
6.3 Mineralized shears .................................................................................................... 64
6.4 Discussion of alteration minerals & chemical gradients ........................................... 65
7 NI LATERITE ....................................................................................................................... 67
7.1 Introduction............................................................................................................... 67
7.2 Methodology ............................................................................................................. 67
7.3 Results ....................................................................................................................... 68
7.4 Discussion .................................................................................................................. 73
8 PHOSPHATE ....................................................................................................................... 75
8.1 Introduction............................................................................................................... 75
8.2 Methods .................................................................................................................... 75
8.2.1 Research rationale and background ................................................................... 75
8.2.2 Sampling ............................................................................................................ 76
8.3 Results ....................................................................................................................... 76
8.4 Discussion .................................................................................................................. 78
9 REFERENCES/LITERATURE CITED ....................................................................................... 79
Appendix 1: Microprobe Data ................................................................................................. A-1
Appendix 2: Multi-element geochemistry ............................................................................ A-12
Appendix 3: Petrographic Descriptions ................................................................................ A-14
Appendix 4: SWIR & TIR Spectra of apatite (Mitchell collection) ......................................... A-52
Appendix 5: Sample Catalogue ............................................................................................. A-58
v
LIST OF FIGURES
Figure 2-1: BSE images of poly-phase epidote-clinozoisite ........................................................ 6
Figure 2-2: Histogram of epidote and clinozoisite microprobe compositions from all M400
gold sites ..................................................................................................................................... 7
Figure 2-3: Epidote, clinozoisite and chlorite compositional relationships ................................ 9
Figure 3-1: Amphibole paragenesis from BSE images. ............................................................. 12
Figure 3-2: Foliation- and vein-hosted Al-amphibole (tschermakite) ....................................... 13
Figure 3-3: Amphibole composition plot of metamorphic, Al-amphibole and Si-amphibole .. 14
Figure 3-4: BSE images of vein-hosted, coexisting epidote and amphibole phases ................. 15
Figure 3-5: Amphibole determination from SWIR at Bullant and Wattle Dam deposits ........ 17
Figure 3-6: Correlation of whole-rock Mg % with SWIR 2330 feature ..................................... 18
Figure 3-7: Amphibole spectral classification scatter plots ...................................................... 19
Figure 3-8: Back-Scattered Electron (BSE) images of metamorphic amphibole (Act) ............. 20
Figure 3-9: BSE images of minerals and textures typical of the Si-amphibole assemblage ..... 20
Figure 3-10: UDD1510, Plutonic: 2330 nm feature (W2330) vs depth. .................................... 21
Figure 4-1: Location of Victory-Defiance section ...................................................................... 25
Figure 4-2: Leapfrog® model of Victory-Defiance section, looking to NW. .............................. 26
Figure 4-3: Location of diamond holes used to construct Victory-Defiance section ................ 27
Figure 4-4: Leapfrog® model showing vertical alteration zoning at East Repulse. ................... 29
Figure 4-5: CD5026 Distribution of chlorite, amphibole, talc and dark micas ......................... 29
Figure 4-6: Leapfrog® model showing distribution of clinozoisite - epidote ........................... 30
Figure 4-7: Distribution of epidote and magnetite in CD6800 ................................................. 31
Figure 4-8: Leapfrog® model looking ~NNW showing distribution of anhydrite/gypsum ....... 31
Figure 4-9: CD7068: Oxidized mineral assemblages ................................................................ 32
Figure 4-10: Summary of mineral paragenesis relative to timing of gold deposition .............. 33
Figure 4-11: δ34Spyrite across Victory - Defiance section ........................................................ 35
Figure 4-12: δ13Ccarbonate across Victory - Defiance section .................................................. 35
Figure 4-13: Spectral and isotopic properties of CD5026 ......................................................... 37
Figure 4-14: Spectral and isotopic properties of CD4997. ........................................................ 38
Figure 4-15: Spectral and isotopic properties of CD6024 ......................................................... 39
Figure 5-1: Wallaby deposit and environs ................................................................................ 41
Figure 5-2: Magnetic map of the Wallaby deposit and environs .............................................. 42
Figure 5-3: Paragonite, muscovite & phengite distribution in the Wallaby hinterland............ 43
Figure 5-4: Relative timing of magmatic, deformation and alteration events ......................... 45
Figure 5-5: Biotite to dolomite - albite - pyrite zoning ............................................................. 45
Figure 5-6: View of SWIR & isotope data in Leapfrog® model, upper section Wallaby deposit
.................................................................................................................................................. 46
Figure 5-7: Location, lithology and alteration zoning of WB801CD .......................................... 47
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Figure 5-8: WB0801CD oxidized alteration assemblages .......................................................... 49
Figure 5-9: WB0801CD reduced and acid alteration assemblages ........................................... 49
Figure 5-10: WB0801CD comparison of gold grades with stable isotopes ............................... 50
Figure 5-11: Photomicrographs of epidote replacement of hornblende F.O.V = 1.5x1mm. .... 50
Figure 5-12: Variation of δ34Spyrite through paragenetic stages of the Wallaby deposit ........ 52
Figure 5-13: δ13Ccarbonate vs δ18Ocarbonate for the Wallaby deposit .................................. 53
Figure 5-14: δ13Ccarbonate vs δ34Spyrite for the Wallaby deposit ........................................... 54
Figure 5-15: Inferred COH speciation from δ13C carbonate and δ34S pyrite ............................ 55
Figure 5-16: Alteration and fluid evolution of the Wallaby deposit ........................................ 58
Figure 5-17: Redox/pH conditions of formation the Wallaby Deposit...................................... 59
Figure 6-1: Leapfrog® model looking to the northwest ............................................................ 62
Figure 6-2: Leapfrog® model looking to the northeast ............................................................. 62
Figure 6-3: Leapfrog® model looking to the north A: Au grades B. Metasomatic amphibole .. 63
Figure 6-4: Leapfrog® model A: Prehnite B. Amphibole (squares) with prehnite (spheres) .... 63
Figure 6-5: Leapfrog® model A: Epidote-clinozoisite B: Biotite C. Anhydrite-gypsum.............. 64
Figure 6-6: Chemical gradients in the Bullant Au system ......................................................... 65
Figure 7-1: Scatter plots with Principal Component (covariance) bands 2 and 5 ..................... 69
Figure 7-2: Scatter plots with Principal Component (covariance) bands 7 and 9 ..................... 71
Figure 7-3: Line graphs showing variation in RSE with respect to sample size (rate). .............. 72
Figure 8-1: End-member classification from PCA Vs whole-rock % P2O5 plots ......................... 77
Figure 8-2: Spectra representative of VNIR end-member classification ................................... 77
Figure 8-3: Ratio of depths of 2212 and 1932 nm features (d2212/1932) vs % P2O5 ............... 78
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EXECUTIVE SUMMARY
Focusing on the Eastern Goldfields of Western Australian, the objectives of the M400 research were to:
Validate existing HyLogging mineralogical results
Collaborate with mine-site staff to equip them with skills in HyLogging mineralogical
interpretations, software use, and interpreting chemical architectures implied by their deposit
samples
The major achievements of the project were to:
Place the HyLogging results within the context of Archean gold mineral systems
Mineralogically and spatially validate the significance of interpreted hydrothermal
assemblages; developing 3D models at Victory-Defiance, Wallaby and Bullant Au deposits
Assist knowledge transfer to the Au, Ni and phosphate industries
The project focused on the hydrous silicate alteration mineralogy associated with gold mineralization.
New TSG®1 scalars
2 were developed to differentiate clinozoisite from epidote and hydrothermal Al-
amphiboles from hydrothermal Si-amphiboles and metamorphic amphiboles. These scalars were
validated by petrographic observations, electron microprobe analyses and whole rock geochemical data.
The new TSG® scalars were employed in hyperspectral alteration mapping in conjunction with existing
capacity of TSG®. Case studies that illustrate the relationship of mineralogical zoning to Au
mineralization are documented for the Victory-Defiance Complex, St Ives Camp, the Wallaby deposit
and the Bullant deposit. Correlations between stable isotopic characteristics and silicate mineralogy, as
mapped by SWIR3 HyLogger/HyChips technologies, confirm that systematic changes in the silicate
alteration mineralogy reflect changes in the redox state of Late Archean Au systems, and associated
changes in fluid acidity. A broad subdivision of chemical conditions of formation of the hydrous silicate
± oxide ± sulfide assemblages is as follows:
Clinozoisite - chlorite ± pyrite ± pyrrhotite assemblages reflect reduced and acidic conditions
Al-amphibole assemblages reflect reduced and near neutral to alkaline conditions
1 The Spectral Geologist (TSG®) is a specialist processing and analysis software package designed for
analysis of field or laboratory spectrometer data
2 TSG® uses the term scalar to refer to any set of imported or calculated values associated with the
spectral data
3 SWIR: Short wavelength infrared spectroscopy
viii
Epidote ± magnetite ± pyrite and anhydrite ± phlogopite assemblages reflect oxidized
conditions and near neutral to alkaline conditions
Si-amphibole ± phlogopite reflect oxidized, transitional to reduced conditions at alkaline
conditions
Mutually overprinting paragenetic relationships between clinozoisite and epidote as well as biotite,
amphibole and chlorite suggest that the development of the reduced and oxidized assemblages
overlapped in time. The redox and associated pH gradients are spatially related to gold occurrences.
Both the mineralogical and isotopic patterns provide opportunities to map from barren to productive
parts of Au systems.
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ACKNOWLEDGMENTS
The authors would like to thank the sponsors of the M400 project; MERIWA and CSIRO Minerals
Down Under Flagship, and government and industry partners Geological Survey of Western Australia,
Heron Resources, Vale Australia, Kalgoorlie Consolidated Gold Mines, Kanowna Belle Gold Mine,
Darlot Gold Mine, Granny Smith Gold Mine, Lawlers Gold Mine, Plutonic Gold Mine and St Ives Gold
Mine for their added logistical and in-kind support.
Special thanks also go to Kai Yang and Mel Quigley for their spectral geology and 3D modelling
expertise, Peter Mason for TSG-related advice, Lew Whitbourn for HyChips support and Cheryl Harris
for help with final report corrections.
1
1 INTRODUCTION
1.1 OBJECTIVE OF MERIWA M400
With drilling costs accounting for up to 40% of total exploration expenditure and 5-10% of mine
production costs, gaining increased value from drilling is critical to reducing costs and improving
productivity. With foreseen shortages in experienced industry professionals, adoption of new skills and
assistance from new technologies is also seen as imperative to sustainable discovery. The aim of this
project was to increase the returns from drilling by embedding a new layer of mineralogical
understanding and associated geochemical concepts into a wide group of Australian mining and
exploration business units and SMEs.
M400 focused on the Western Australian Goldfields, building on the advances of MERIWA projects
M3584, M373
5 and M377
6 and utilising the expertise of a new Regional HyLogging Researcher based
at Kalgoorlie. The objectives of the research were:
To validate existing HyLogging mineralogical results from each sponsor by means of QXRD,
electron microprobe and petrological methods
To collaborate with mine-site staff to equip them with skills in HyLogging mineralogical
interpretations, software use, and interpretation of chemical architectures implied by their
deposit samples.
To up-skill mine site staff with new procedures and competencies.
1.2 METHODOLOGY
For twenty years mineral exploration has used SWIR hyperspectral data in the search for resources
(Hauff et al., 1989; Herrmann et al., 2001; van Ruitenbeek et al., 2005), but fresh-rock alteration
4 M358: Scale-integrated, architectural and geodynamic controls on alteration and geochemistry of gold
systems in the Eastern Goldfields Province, Yilgarn Craton
5 M373: Development and implementation of advanced automated core logging technology for
enhanced mine feasibility and development in Western Australia
6 M377: Scale-integrated, architecturally, geodynamically and geochemically constrained targeting
models for gold deposits in the Eastern Goldfields Province, Yilgarn Craton
2
mapping over this period has been predominantly restricted to white mica and to a lesser degree
chlorite. White mica composition is the most well accepted hyperspectral index for characterizing
alteration (Scott and Yang, 1997), but where white mica is present only in small amounts, lithologically
and metamorphic dependent proxies for other alteration minerals must be used. Chlorite composition
(Pontual et al., 1997) is another spectral index that is used to differentiate proximal from distal
alteration, and within Archean gold provinces may be used in tandem with white mica composition to
effectively map alteration (Halley and Walshe, 2006).
M400 aimed to extend the available spectral indices for mapping alteration in Au systems by
characterizing alteration minerals and mineral assemblages that were common to both gold-sponsor
sites. This approach aimed to create a few robustly validated spectral indices rather than a less thorough
validation of scalars for all gold-associated alteration minerals encountered at sponsors’ sites. The
mineral list included clinozoisite - epidote, amphibole, phlogopite, anhydrite, prehnite and chloritoid
and there was a particular focus on clinozoisite - epidote and amphibole assemblages. The list also
reflected the dominance of mafic - intermediate host rocks at sponsors’ sites.
Spectral validation procedures routinely involved:
Stage 1
Characterising minerals, mineral assemblages and mineral compositions through petrographic
descriptions supplemented with electron (BSE) images for additional textural reference, electron
microprobe analyses (EMPA) and X-ray diffraction.
Stage 2
For selected minerals and assemblages of Stage 1, identification of diagnostic absorption feature(s) in
the visible near infrared (VNIR) or shortwave infrared (SWIR), leading to a series of spectral indices,
scalars or classifications.
Stage 3
Integrating spectral scalars with geological and geochemical constraints (lithology, structure, litho-
geochemistry, mineral para-genesis, isotopic data) to define mineral zoning and constrain geochemical
gradients at selected sites. LeapfrogTM
was acquired as part of the project to allow 3D evaluation of
spectral scalars and integration of spectral data into 3D mineral system models.
Stage 4
Writing a tutorial that details how each scalar or classification was created, its significance in terms of
the mineral system understanding, and practical applications for sponsors. Release of the tutorials
coincided with regular workshops/meetings throughout the project.
3
Electron microprobe analyses (M400) were obtained using a JXA 8200 EPM at James Cook University,
Townsville, using 15 kV acceleration voltage, 20 nA probe current and Jeol CITZAF (based on
Armstrong method matrix correction). Additional analyses (Bil, 2010) were obtained from a SEM-EDS
Hitachi S-4700 with Thermo Noran Vantage analytical system at the Institute of Earth Science,
Jagiellonian University, Cracow and a FEI Quanta 200 FEG with Schattky field emission gun at the
Department of Economic Geology, AGH University, Cracow. Both Polish SEM devices used 15 kV
acceleration voltage and 10 nA probe current. Oxide totals are expressed as wt%.
The Spectral GeologistTM
(TSGCoreTM
) software was used for spectral interpretation and scalar
construction.
Multielement analysis was undertaken at ALS Chemex Perth using Method ME-MS61. This comprised
pre-digestion of a 0.5 g sample for 10-15 minutes in a mixture of nitric and perchloric acids, followed
by the addition of hydrofluoric acid that was then evaporated to dense perchloric fumes (incipient
dryness). The residue was leached in a mixture of nitric and hydrochloric acids, then cooled and diluted
to a final volume of 25 mls. Elemental concentrations are measured using ICP Atomic Emission
Spectrometry and ICP Mass Spectrometry.
1.3 TRAINING WORKSHOPS AND ON-SITE INSTRUCTION
The list of activities, summarized from quarterly reports, records the contribution by M400 to
collaborating with mine-site staff to equip them with skills in HyLogging mineralogical interpretations,
software use and understanding and application of chemical gradients in mineral systems.
January-February 2008, GSWA Kalgoorlie: HyChips measurement based at GSWA Kalgoorlie
saw St Ives diamond core logged spectrally. The spectra were used in M400 to develop
indices, map alteration across the Victory - Defiance Complex and define district-scale
chemical gradients. Training and technical support was provided for this sampling campaign.
March 2008, KCGM coreyard: James Davis of St Ives received 2 days training on HyChips 6-4
and on the formulation of spectral indices. A one day visit to St Ives combined a collaborative
assessment of the logistics of getting spectral indices into site-based databases and mining
software.
March 2008, KCGM: The first formal training workshop was held at the KCGM computer
training rooms in Kalgoorlie on March 27th and 28th and was attended by 12 sponsor
4
participants. The two days of training included spectra measurement with the HyChips 6-4
instrument at the KCGM Core Library, TSG spectral processing and mineralogical
interpretation provided by Jon Huntington and Peter Mason, and supported by Cajetan Phang,
Lee Durrant and Tony Roache. John Walshe gave an overview presentation on the rationale
for the use of spectral mineralogy in ore systems understanding.
April 2008, KCGM coreyard: Training during the KCGM M400 spectra collection involved
instruction of new staff in the operation of HyChips 6-4, ongoing measurement advice, some
data checking and general support. Time was also spent providing technical support for
HyChips operating problems, including testing and diagnosing faults in operator procedures,
hardware and software. This entailed re-setting table position, and installing additional roller
racks for safety and operator ease. Support also included the installation of a new hard disk for
the HyChips computer, new versions of LabVIEW® 4_9 software, and time in testing the new
soft/hardware.
July 2008, Barrick Perth office: A two day meeting and TSG workshop was held on July 30-
31st. Jon Huntington and Peter Mason were the principal conveners.
August-September 2008, KCGM offices and GSWA Kalgoorlie: TSG training/guidance was
planned with KCGM geologist Vanessa Beach for August, and was followed up with a half day
training/guidance. HyChips training for GSWA was planned and was followed by
measurement and training for Chris Kojan during September.
March 2009, GSWA Kalgoorlie: The third M400 workshop involved 2 days of presentations of
findings to date and a half day TSG workshop.
April-May 2009, GSWA Kalgoorlie and KCGM coreyard: KCGM collected HyChips spectra
from chips and core from within the Fimiston Pit as part of their exercise in interpreting
mineralogy from spectra to improve grade control practices, including ore boundary
delineation. A KCGM geologist, Eric Hein, was trained to collect spectra from HyChips,
including protocols in QA/QC. A TSG® refresher was given to mine geologist Rebecca
Burgess on processing the spectra. The diamond holes were used to validate mineralogical
interpretation from the chips spectra, which involved alteration logging, geochemical sampling,
and the selection of the most pertinent textural examples for petrography.
July 2009, Carlisle Core Library: The fourth M400 workshop incorporated the presentation and
discussion of results from the project to date, including the roll-out of spectral index tutorials,
and the mid-project meeting that allowed sponsors to give feedback on progress to date and
research/training suggestions for the remainder of the project.
December 2009, St Ives Minesite: Presentation of epidote-clinozoisite characterization, spectral
validation and potential applications to St Ives.
5
2 CLINOZOISITE – EPIDOTE
2.1 INTRODUCTION
Epidote and clinozoisite have both been recognized as metasomatic alteration minerals in the Archean
Yilgarn Craton in this study. Clinozoisite had previously been recognised as a alteration mineral at St
Ives (Clark et al., 1989). Detailed sampling and analyses at each of the seven M400 study sites revealed
that clinozoisite is a common metasomatic phase at most sites, and is also spatially and temporally
related with one of the dominant styles of gold mineralization at the Plutonic gold mine. Clinozoisite -
epidote were chosen as prospective minerals to spectrally characterize due to a diagnostic, well-
developed absorption feature at approximately 1550 nm shared only by the two minerals. The aim of
using the 1550 nm absorption feature was to develop a single parameter that could record the
distribution of previously unlogged clinozoisite and differentiate between areas dominated by either
clinozoisite or epidote. This mineralogical distinction is important as Au mineralization is related
spatially and temporally to the switch from epidote stable to clinozoisite stable assemblages.
2.2 TEXTURAL & PARAGENETIC INTERPRETATION
A set of textural criteria was devised to distinguish between clinozoisite, epidote and associated
minerals of hydrothermal and metamorphic origin. Classification of alteration minerals related to
metasomatic events, as opposed to “metamorphic minerals”, was based on the association with vein
assemblages. Matrix-hosted alteration minerals and/or assemblages that may otherwise have been
defined as “metamorphic” assemblages were classified as metasomatic-related if grains were:
fractured, in-filled and commonly accompanied by brecciation
contained within the selvage to veins
patchy overgrowths associated with veins
of similar composition, at least at the rims, and habit to grains within adjacent veins.
Mineral compositions used in conjunction with textures lend greater confidence to differentiation of
alteration minerals and metamorphic minerals that grew in response to variable metamorphic conditions
or within contrasting lithologies. Diagnostic mineral habits in combination with mineral associations
and compositional groupings may aid definition of mineral paragenesis within deposits and link similar
mineral associations between deposits.
6
Given these criteria, the parageneses of epidote and clinozoisite with respect to metamorphic amphibole
and plagioclase may be summarized as follows:
Metamorphic actinolite and/or plagioclase (oligoclase) were replaced by epidote;
Metamorphic hornblende and/or calcic plagioclase (bytownite) altered to clinozoisite;
Within tschermakite-bearing rocks, clinozoisite is the main epidote-series phase;
Epidote is only present within tschermakite-bearing rocks where it was overgrown by the latter
If there is neither clinozoisite nor any preserved metamorphic actinolite cores within a
tschermakite-bearing sample, there is no epidote overprint.
Where epidote-bearing veins overprint metamorphic hornblende or calcic plagioclase, epidote generally
rims clinozoisite within the wall-rock (eg. Figure 2-1a), or in some circumstances may be rimmed by the
latter (eg. Figure 2-1b). Commonly chlorite and quartz are associated with clinozoisite replacement of
epidote and albite + K-spar ± muscovite is associated with epidote replacement of clinozoisite. In
extreme cases, mutually overprinting vein-hosted epidote and clinozoisite are associated with
oscillatory-zoned epidote-clinozoisite grains (Figure 2-1c).
Figure 2-1: BSE images of poly-phase epidote-clinozoisite
a) Zoned, elongate accumulations of clinozoisite (Czo) and epidote (Ep) are surrounded by actinolitic
hornblende (Act-Hb). Sample M400-098; Darlot. b) Zoned clinozoisite (Czo) and epidote (Ep) after
bytownite (Pl). Epidote is concentrated within veins that also contain chlorite (Chl) and calcite (Cc). Sample
M400-079; Lawlers. c) Bytownite was cross-cut by oligoclase (Oligo) - bearing veins that are also associated
with oscillatory-zoned epidote (Ep) and clinozoisite (Czo). Sample M400-073; Lawlers.
7
2.3 HYPERSPECTRAL INDICES AND MINERAL COMPOSITIONS
As deduced from a US Geological Survey Spectral Library (Clark et al., 2007) epidote and clinozoisite
short wave infrared (SWIR) spectrum, the 1550 nm absorption feature of epidote has a relatively short
wavelength when compared to clinozoisite. A threshold of 1554 nm was selected to distinguish
between epidote (<1554 nm) and clinozoisite (>1554 nm). Even with the 1550 nm wavelength
distinction there is interference in using this parameter from minerals such as chlorite and amphibole;
therefore an additional parameter was formulated to select only the most intensely developed 1550 nm
feature. The combination of these two parameters results in the selection of high-abundance epidote-
and clinozoisite-bearing rocks that are usually represented by vein infill and the exclusion of samples
with excessive amounts of amphibole and chlorite that create ambiguity in the clinozoisite-epidote
distinction.
Figure 2-2: Histogram of epidote and clinozoisite microprobe compositions from all M400 gold sites
Compositons expressed in epidote molecule content pistazite (Ps) or Fe3+/(Fe3++Al)*100. Compositions
collectively define a broadly bimodal distribution with the main populations bisected by a threshold of 15 Ps,
which from the literature corresponds to the distinction between end member phases. Deposits: St Ives;
Plutonic; Bullant; Darlot; KCGM; Lawlers; Granny Smith. Analyses documented in Appendix 1.
8
Epidote-clinozoisite microprobe compositions from all M400 gold sites collectively define a broadly
bimodal distribution (Figure 2-2). Each population is approximately separated by an epidote molecule
content pistazite (Ps) of 15. A Ps value of 15 is stated in the literature to distinguish epidote (>15) from
clinozoisite (<15).
Validation of the clinozoisite and associated spectral parameter was by XRD, petrography and electron
microprobe analysis (EMPA). Epidote-clinozoisite microprobe compositions from the seven gold
deposits collectively define a broadly bimodal distribution (Figure 2-3). Each population is
approximately separated by an epidote molecule content pistazite (Ps) of 15. A Ps of 15 distinguishes
epidote (>15) from clinozoisite (<15) (Deer et al., 1997). Observations from pure epidote and
clinozoisite spectra (Clark et al., 2007) reveal that a change in the position of the 1550 nm absorption
feature from relatively low to high wavelengths is related to a shift from epidote to clinozoisite,
respectively. Other mineral spectra – including chlorite – that contain a weak absorption feature at 1550
nm may be filtered out using the depth of the latter, as epidote and clinozoisite contain a relatively deep
1550 nm absorption feature. The combination of the wavelength position and depth of the 1550 nm
absorption feature – defined here as the epidote-clinozoisite index – is used to spectrally characterize the
epidote-clinozoisite solid solution series. Comparison of the epidote-clinozoisite index with epidote
and/or clinozoisite compositions yields a subdivision of epidote- and clinozoisite-bearing samples based
on a threshold of 1552.5 nm (Figure 2-3a). Inconsistencies in the classification are related to samples
that contain both epidote and clinozoisite, as indicated by the spread of EMPA compositions in some
samples. Petrography reveals that regardless of the EMPA compositional range, samples classified as
epidote and clinozoisite on the basis of the epidote-clinozoisite index predominantly contain the
corresponding phase. In many cases the subordinate phase represents relict porphyroblast cores (Figure
2-1a) and/or isolated veins (Figure 2-1b). Epidote and clinozoisite commonly coexist with chlorite
within mafic rocks; therefore in an effort to draw paragenetic links between end-member mineral phases
that have been hinted through petrographic observation and EMPA compositions, epidote-clinozoisite
and chlorite composition indices were compared from samples that only contain coexisting chlorite
and/or clinozoisite. Correlation of indices shows that epidote and clinozoisite coexist with Mg-rich
chlorite and Fe-rich chlorite, respectively (Figure 2-3b).
9
Figure 2-3: Epidote, clinozoisite and chlorite compositional relationships
Data from the seven studied gold deposits within the eastern Yilgarn Craton.
a) Scatter plot of (Fe3+/[Fe3++Al]*100) – epidote molecule content pistazite (Ps) – versus the epidote-
clinozoisite index (w1550). Wavelength in nanometres (nm). Classification of epidote (Ep) and clinozoisite
(Czo) is differentiated by a threshold value of 1552.5 nm. Samples circled by stippled line fall outside of the
classification scheme where: samples that contain values below or near to 15 Ps within the epidote domain
represent subordinate clinozoisite (Figure 2-1a) and samples with values above 15 Ps within the Czo domain
represent subordinate epidote (Figure 2-1b). Al and Fe3+ were calculated on the basis of 12.5 O.
b) Scatter plot of the chlorite composition index (w2250) versus the epidote-clinozoisite index (w1550).
Wavelength in nanometres (nm). Samples selected for comparison contained chlorite and
epidote/clinozoisite. Thresholds of 2255 nm and 1552.5 nm differentiate epidote (Ep) and Mg-rich chlorite
(Mg-Chl) from clinozoisite (Czo) and Fe-rich chlorite (Fe-Chl). Most samples fall within each mineralogical
domain.
2.4 DISCUSSION
Epidote and clinozoisite compositions predicted from spectral analysis of multi-phase epidote- and
clinozoisite-bearing samples do not match the broad compositional ranges measured by EMPA. The
most likely reason for this is that the SWIR spectra were derived from a large area (1 cm diameter)
compared to the EMPA spot size. An averaged SWIR spectrum per sample was plotted against the
range of EMPA compositions from the one sample, therefore eliminating the subjectivity in assigning
variable epidote-clinozoisite index values to particular EMPA analyses. The apparent inconsistency in
the assignment of epidote and clinozoisite to their respective domains would be improved by reducing
the diameter of the hyperspectral lens to approach the spot size of the EMPA, but in terms of applying
the epidote-clinozoisite index to mapping at drill hole, mine and exploration scales, the general
correlation between SWIR and EMPA is more than sufficient to delineate broad alteration domains.
Differentiation between metamorphic- and metasomatic-derived epidote-clinozoisite may require the
mapping of structurally controlled fluid pathways (Roache, 2008) combined with lithogeochemistry, but
the increasing integration of mineralogically validated hyperspectral indices – as shown by the
correlation of chlorite composition and epidote-clinozoisite indices – will result in a robust measure of
metasomatic mineral assemblages that uniquely map Archean mineral system architecture.
10
11
3 AMPHIBOLE
3.1 INTRODUCTION
Two types of hydrothermal amphibole, each with its own variation in textural style and associated
minerals, are characteristic of most gold deposits studied in M400, and represent one of the most
abundant and widespread alteration styles that is spatially and/or temporally associated with gold
mineralization. These two types of calcic amphibole are termed Si-amphibole and Al-amphibole in this
report. Si-amphibole encompasses the compositional fields of tremolite, actinolite and ferro-actinolite
and Al-amphibole encompasses the compositional fields of Al-rich hornblende, tschermakite and ferro-
tschermakite. The terms Si-amphibole and Al-amphibole are also used as standard prefixes to refer to
associated mineral assemblages and alteration events; e.g. a Si-amphibole event or Al-amphibole
assemblage.
The Al-amphibole assemblage contains tschermakite + Ca-plagioclase (up to bytownite) ± titanite ±
quartz. Al-amphibole is common to Plutonic, St Ives, Darlot and Lawlers Au deposits. The Si-
amphibole assemblage includes chlorite + K-feldspar + albite ± actinolite / tremolite ± quartz ±
carbonate ± garnet ± anhydrite ± talc. The Si-amphibole assemblage is vein-hosted, and has a
commonly pervasive selvage that replaced and cross-cut metamorphic minerals. Si-amphibole is
common to all M400 gold sites.
Gold mineralization is associated with the intersection of Al-and Si- amphibole assemblages in addition
to several other minerals including biotite ± prehnite ± fluor-apatite as well as sulphide phases including
arsenopyrite with gold-bearing inclusions at Plutonic. Within fluor-apatite bearing samples the former
may contain up to 4 Wt% F, and coexisting hornblende and biotite may contain up to 1 Wt% F.
3.2 TEXTURAL & PARAGENETIC INTERPRETATION
Hydrothermal and metamorphic amphiboles were differentiated using the textural criteria discussed in
section 2.2. Metamorphic amphiboles typically form patchy aggregrates or porphyroblasts that are
fractured and rarely zoned (Figure 3-1a). The origin of zoning is ambiguous. Amphiboles of actinolite
to hornblende composition, that form cores to all other amphiboles, are assumed to be of metamorphic
(or igneous) origin, without textural evidence to the contrary. Where there is textural context between
Al-amphibole that has a characteristic bladed crystal habit arranged within radial aggregates, and
12
texturally diagnostic metamorphic amphibole, the Al-amphibole consistently overprints the
metamorphic amphibole (Figure 3-1b). In Figure 3-1c a similar relationship occurs between bladed Al-
amphibole and porphyroblasts of metamorphic amphibole but both phases are fractured and infilled by
vein-hosted Si-amphibole. Where the Al-amphibole and vein-hosted Si-amphibole are in direct textural
contact, the latter partially replaces the former so as to leave isolated grains of Al-amphibole within
cores of amphibole aggregates. The crystal habit and grain configuration of Al-amphibole serves as a
diagnostic feature preserved where intensely developed and vein-related Si-amphibole has replacement
Al-amphibole (Figure 3-1d). In such cases, relict tschermakitic core compositions were altered to
actinolite but are slightly more aluminous than comparatively tremolitic actinolite-bearing rims.
Figure 3-1: Amphibole paragenesis from BSE images.
a) Hornblende (Hb) porphyroblast that has gradational boundaries to actinolite (Act) that in turn shares a
sharp contact with outermost tschermakite (Ts). Actinolite within fractures cross-cut the hornblende core
that partially extend from patchily-intergrown actinolite+tschermakite on the right side of the image.
Sample M400-062; Lawlers. b) Relict hornblende (Hb) cores are rimmed by tschermakite (Ts) that is
adjacent to radial clusters of tschermakite. Sample M400-060; Lawlers. c) Actinolite (Act) cross-
cut/replaced Hb within a linear segment on the top-half of the amphibole porphyroblast, and also replaced
radially-arranged Ts that lie within the core of the porphyroblast. Sample M400-082; Darlot. d) Actinolite
(Act1) is rimmed by Act2. Sample M400-128; Bullant.
13
Figure 3-2: Foliation- and vein-hosted Al-amphibole (tschermakite)
a) Scanned image of thin section with locations of BSE images in relation to foliations and inter-folial zones.
Sample M400-116; St Ives. b) BSE image of prismatic actinolite (Act) surrounded by calcite (Cc). c) BSE
image of elongate amphibole lathes with subtle compositional zonation delineating hornblende (Hb) cores
and tschermakite (Ts) rims. d) Photograph of halved NQ core containing tschermakite-bearing veins and
clinozoisite selvage within dolerite. Sample M400-Dar059; Darlot.
Microprobe-derived compositions and textures show that hornblende-tschermakite is restricted to
foliations, whereas outside of foliation zones actinolite is randomly oriented and prismatic compared to
the foliation-defining Al-amphibole (hornblende-tschermakite) lathes (Figure 3-2a-c). Vein-hosted Al-
amphibole has a diagnostic texture in hand specimen (Figure 3-2d). Composites of the small-scale
foliations and veins may form macroscopic-scale structures that can be tens of metres in width.
Tschermakite is contained within veins, selvage to veins and rims of pre-existing grains, but in the case
of the latter, textures do not independently differentiate alteration from metamorphism.
The amphibole compositional data were subdivided on the basis of the textural criteria described in
section 2.2. Metamorphic amphibole occupied most of the compositional space except for the extremes
including Mg-rich tremolite, ferro-actinolite and apart from three anomalous analyses (one sample),
tschermakite (Figure 3-3). Due to the strict textural criteria used for the classification, many of the
amphibole analyses classified as metamorphic – including the three isolated metamorphic tschermakite
analyses – may in fact be hydrothermal. Metamorphic amphibole of actinolite composition (7.5-8.1 Si)
14
is associated with oligoclase, whereas amphibole of hornblende composition (6.5-7.25 Si) is associated
with labradorite. Al-amphibole is predominantly characterized by tschermakite that varies between Mg
and Fe end-members. The variation in Mg/(Mg+Fe2+
) content is primarily dependent on the host
lithology and secondarily controlled by alteration, in that Al-amphibole has higher Fe/Mg than the
precursor amphibole. Variation in the Si (and Al) content of Al-amphibole is controlled by the intensity
of alteration. Si-amphibole is mainly confined to actinolite compositional space, but there is a larger
range in Mg/(Mg+Fe2+
) due to a tendency of the former to alter metamorphic tremolite to relatively
higher Mg/(Mg+Fe2+
) and alter ferro-tschermakite to ferro-actinolite.
Figure 3-3: Amphibole composition plot of metamorphic, Al-amphibole and Si-amphibole.
Amphibole analyses documented in Appendix 1.
There are few examples of where all of the contrasting vein-hosted mineralogy and textural variations
can be observed in one sample, but one such example shows that all of the usually disparate and
ambiguous mineral relationships may be explained within a single textural framework as part of a series
of multiply oriented, chlorite-, plagioclase-, epidote- and amphibole-bearing veins (Figure 3-4a). Veins
that protrude from the edges of large actinolite grains predominantly contain randomly to un-oriented,
subhedral, zoned hornblende-actinolite and plagioclase, unzoned epidote, minor chlorite, and rims of
Ca-rich plagioclase of up to labradorite composition adjacent to a prehnite + chlorite + albite +
15
Figure 3-4: BSE images of vein-hosted, coexisting epidote and amphibole phases.
Sample M400-054; Lawlers. a) An actinolite (Act) porphyroblast with tschermakite (Ts) rims is also cross-
cut by multiply-oriented veins such as shown within figure 1d (inset). Chlorite (Chl) is the dominant matrix
phase. Locations of figures 9b&c and 9d and the vein they encompass are shown by insets in the top left of
the image. b) Bright BSE image to show feldspar compositional variation across the vein. Spheroid-shaped
plagioclase (Pl) grains with relatively Ca-poor cores and Ca-rich rims formed tightly-packed accumulations
within the centre of the vein. Relatively Ca-poor plagioclase that is interstitial to zoned plagioclase grains
forms an inner zone, and relatively Ca-rich plagioclase, or labradorite (Lab), forms an outer rim to the vein.
c) BSE image of the same area as in figure 9b, but with relatively low brightness. Zoned actinolite (Act) and
tschermakite (Ts,) and unzoned epidote (Ep) mutually overprint each other and are irregularly-distributed
with respect to vein-hosted plagioclase. d) BSE of a section of vein adjacent to the actinolite porphyroblast,
with low brightness to emphasize amphibole and epidote compositional variation. Epidote and zoned
tschermakite+actinolite form alternating layers, with each successive layer overprinting the last. Amphibole
grains in particular show a preferred orientation perpendicular to the vein wall. An outermost epidote grain
shows anomalous compositional change to relatively Al-rich epidote where part of the grain protrudes past
the labradorite rim, which forms the edge of the vein.
muscovite matrix (Figure 3-4b&c). In contrast, at the intersection of veins and actinolite
porphyroblasts, oriented hornblende-actinolite and epidote within the veins project outwards from the
porphyroblast surface towards the vein rim (Figure 3-4d). Epidote and zoned hornblende-actinolite are
roughly distributed within alternating layers so that the outer margin of each mineral within a layer was
overprinted by a succeeding mineral, which is distinct from a laterally extensive unconformable surface.
Epidote that defines the outermost of these layers and that straddles the vein-matrix boundary differs
from epidote wholly contained within veins because it is marked by a gradual change in composition
16
either side of that boundary. The range of compositions from 10.5 to 7.8 wt% FeO is dependent upon
whether epidote is vein- or matrix-hosted, respectively.
3.3 HYPERSPECTRAL INDICES AND MINERAL COMPOSITIONS
Al-amphibole has been recognized as an important gold-related alteration phase within M400 and past
research projects (Roache, 2008). It is predominantly characterized by two spectral indices:
Depth of the 2390 feature (D2390); and
Ratio of 2330 and 2250 feature depths (DMgOH/DFeOH).
The two features tend to complement each other. The DMgOH/DFeOH is useful in moderate to Fe-rich
environments but fails in high Mg-rich environments as the FeOH feature diminishes. The D2390
feature is useful in Mg-rich environments but for reasons that are not clear is diminished in the more Fe-
rich environments.
The amphibole relationship to these contrasting indices is best summed-up in the following deposit
examples in which Al-amphibole is closely associated with gold mineralization:
Wattle Dam mineralization is characterized by the depth of the 2390 feature (D2390); and
Bullant mineralization is characterized by the ratio of 2330 and 2250 feature depths
(DMgOH/DFeOH).
Threshold values of 0.05 for D2390 and 3 for DMgOH/DFeOH were selected to differentiate
metamorphic from Al-amphibole at Wattle Dam and Bullant, respectively (Figure 3-5). The only
identified spectral index that appears related to the D2390 feature and DMgOH/DFeOH ratio of Al-
amphibole is the 2330 feature (W2330). At low values of W2330, Al-amphibole is detected by D2390
and at high values of W2330, Al-amphibole is detected by DMgOH/DFeOH.
The W2330 feature is negatively correlated with whole-rock Wt% Mg (Figure 3-6; Appendix 2). For the
moderate to low amphibole contents, defined from petrography, there is linear trend of negative slope
between W2330 and Wt% Mg. Amphibole content determined from petrography shows that samples
with relatively high amphibole contents plot off the dominant linear trend defined by samples with
moderate to low amphibole contents (Appendix 3). A notable exception to this rule includes one
dominantly amphibole-bearing sample where the amphibole grains were partially carbonatized.
17
Figure 3-5: Amphibole determination from SWIR at Bullant and Wattle Dam deposits
Scatter plots of the depth of the SWIR 2390 feature (D2390) and the depth ratio of the SWIR 2330 and 2250
features (dMgOH_dFeOH) against drill hole depth, as a proxy for amphibole distribution down-hole. Sample
points are coloured by Au (ppm). a) D2390 against depth (m), drilled through the type 1 amphibole-hosted
ore body (>0.5 D2390) into the talc+serpentine-dominated footwall rocks at Wattle Dam. b) D2390 against
depth (m) at Wattle Dam, drilled predominantly through the metamorphic amphibole-rich hangingwall to
the type 1 amphibole-hosted lode position (>0.5 D2390). c) Type 1 amphibole that is spatially-associated with
gold mineralization at Bullant; defined by dMgOH_dFeOH >3.
Conversely, a sample containing a relatively low amount of amphibole compared to samples with
similar Mg%:W2330 has amphibole only second in abundance to plagioclase that is not detectable in
the SWIR. From these observations, the wavelength position of the 2330 feature is controlled primarily
by lithology, and secondarily by amphibole (and/or other mineral/s) content.
Graphic representation of the relationship between D2390, DMgOH/DFeOH and W2330 indices within
tandem scatter plots shows a potential role for W2330 in determining when either amphibole index
should be applied. In the case of D2390, the threshold determined from the Wattle Dam case study is
18
Figure 3-6: Correlation of whole-rock Mg % with SWIR 2330 feature
Correlation plot derived from whole-rock multi-element geochemistry and the wavelength position of the
SWIR 2330 feature (W2330). W2330 was calculated from an average of two spectra taken from thin section
blocks. Sample points are coloured by amphibole abundance (%) within each thin section. Sample 1 contains
carbonatized amphibole and sample 2 contains a comparatively low amount of amphibole, but is second only
to plagioclase in concentration. Samples from Plutonic drill holes UDD1420, UDD1508 and UDD1510.
applicable to samples with W2330 values less than 2325 nm (Figure 3-7a) whereas the threshold does
not apply to Al - amphibole bearing samples above 2325 nm as half of these samples cluster around
0.02-0.03 D2390 and the remaining samples are below 0.01 (masked to 0). For DMgOH/DFeOH, the
Bullant-determined threshold only applies to those samples above approximately 2325 nm, because
many of the samples below 2325 nm contain Fe-poor minerals that do not contain a detectable FeOH
feature in their spectra (Figure 3-7b). The 2325 nm threshold was arbitrarily selected to sub-divide
spectral classification, and given the dataset would have been equally valid between 2318-2327 nm.
Sample points in Figure 3-7 are coloured by EMPA-derived Si, which serves as a proxy for amphibole
composition. As a standard measure, the lowest Si analysis from each sample was assigned to one
VNIR-SWIR spectrum selected for each sample. The discrepancy in scale between SWIR and EMPA
spot sizes is not ideal because of the high degree of microscopic variation in amphibole phases.
Therefore, in cases where Al- amphibole is subordinate to metamorphic amphibole (Figure 3-9a), the
spectral classification would predict the latter even though the sample is compositionally colour-coded
as Al-amphibole (Figure 3-7a). On the other hand, if – assuming the spectral resolution of a HyLogger
or Analytical Spectral Device (ASD) – samples contain an equivalent (Figure 3-9b) or higher amount of
Al- amphibole relative to metamorphic amphibole they will plot within the Al-amphibole field (Figure
3-7b). Another apparent discrepancy in the correlation between amphibole compositions and spectral
19
Figure 3-7: Amphibole spectral classification scatter plots.
Colour legend of %Si applies to both plots. The lowest EMPA-derived Si value for each sample was
correlated with a single VNIR-SWIR spectrum for the same sample. a) Depth of the ~2390 nm feature
(D2390) versus the wavelength position of the ~2330 nm feature (w2330). Amphiboles may be classified into
metamorphic amphibole (<0.05) versus Al-amphibole (>0.05) as long as the corresponding w2330 for each
sample is below the threshold value, here arbitrarily selected as 2325 nm. b) Ratio of the ~2330 nm and
~2250 nm features (2300-2400pfitd/FeOHpfitd) versus w2330. Amphiboles may be classified into
metamorphic amphibole (<3) versus type 1 (hydrothermal) amphibole (>3) as long as the corresponding
w2330 for each sample is above the threshold value, here arbitrarily selected as 2325 nm. Explanation of
numbered samples; point 1 is where Al-amphibole (Si-poor) is subordinate to metamorphic amphibole
(M400-013, Plutonic), point 2 has an equivalent amount of type 1 amphibole relative to metamorphic
amphibole (M400-027, Plutonic), point 3 has a high percentage of type 1 amphibole relative to metamorphic
amphibole (M400-025, Plutonic) and points 4-10 are samples that contain amphibole with a habit similar to
type 1 amphibole, but unlike Si-poor phases it is intergrown with chlorite±epidote±
K-feldspar±albite±prehnite±anhydrite±biotite±talc (4 = M400-024 (Plutonic), 5 = M400-124 (St Ives), 6 =
M400-028 (Plutonic), 7 = M400-010 (Plutonic), 8 = M400-089 (Darlot), 9 = M400-073 (Lawlers), 10 = M400-
106 (Darlot).
classification is those samples that plot within the type 1 amphibole field, but only contain relatively Si-
rich amphiboles. Coarse-grained amphiboles within these samples have a similar habit to type 1
amphibole (e.g. Figure 3-1d) and have Si-poor cores relative to rims, but fine-grained amphibole that is
compositionally identical to rims of the former is intergrown with chlorite± epidote ± K-feldspar ±
albite ± prehnite ±anhydrite ± biotite ± talc (e.g. Figure 3-9a). Fortunately, most of this mineral
assemblage may be characterized in the SWIR, and of these epidote, anhydrite, prehnite and massive
biotite (TSA phlogopite) are highly diagnostic of this assemblage (Figure 3-9b-d). Without the benefit
of the detailed compositional analyses it is possible to use the spectral indices that characterize these
minerals in combination with the D2390 and DMgOH/DFeOH indices to differentiate Al-amphiboles
from samples associated with the Si-amphibole assemblages. Conversely, if Al-amphibole was even
partially replaced by carbonate, chlorite or clinozoisite, the values tend to fall below the respective
thresholds, thus rendering the classification only suitable for the detection of either pristine Al-
amphibole, or where the latter had been replaced by Si- amphibole.
20
Figure 3-8: Back-Scattered Electron (BSE) images of metamorphic amphibole (Act).
Metamorphic amphibole (Act) with type 1 amphibole rims (Hb-Ts). a) Sample M400-013, Plutonic.
b) Sample M400-027, Plutonic.
Figure 3-9: BSE images of minerals and textures typical of the Si-amphibole assemblage.
Back-Scattered Electron (BSE) images: a) A coarse amphibole grain with relict Ferro-hornblende (Ferro-
Hb) cores and actinolite-hornblende (Act-Hb) rims, with the latter having the same composition as relatively
fine-grained, matrix-hosted amphibole that is intergrown with epidote (Ep) and chlorite (Chl). Sample
M400-089 (Darlot). b) Vein containing anhydrite±barite (Anhy+/-Barite) and calcite (Cc), with zoned K’spar
(K’feldspar) and albite (Ab) adjacent to vein walls. Sample M400-082, Darlot. c) Epidote (Ep), prehnite
(Prh), chlorite (Chl), muscovite (lightest shade), K’feldspar (intermediate shade), albite (darkest shade –
black) (Ms+K’spar+Ab) and actinolite (Act) spatially associated with tschermakite (Ts) and calcic
plagioclase (Ca-plag). Sample M400-054, Lawlers. d) Biotite (Bt) grain with albite (Ab) + K’feldspar
(K’spar) reaction rim adjacent to a Ca-plagioclase grain.
21
Application of the new joint index - D2390-DMgOH/DFeOH – is essential within mafic-ultramafic
sequences where there are large fluctuations in the W2330 index. One example of this is at Plutonic,
where lithological variation had previously made it difficult to differentiate the large amount of
metamorphic amphiboles from hydrothermal. As mentioned previously, distinction between the use of
D2390 and DMgOH/DFeOH indices lies in the W2330 index that in the case of Plutonic was at 2320
nm (Figure 3-10). In contrast, the same distinction at Bullant is at 2313 nm. In summary, the W2330
threshold should always be independently defined at each deposit the D2390-DMgOH/DFeOH index is
applied at, and then reassessed according to variations in lithology if the method is to be transferred to
exploration targeting.
Figure 3-10: UDD1510, Plutonic: 2330 nm feature (W2330) vs depth.
Dual scatter plots of the wavelength position of the 2330 nm feature (W2330) against depth down drill hole
UDD1510, Plutonic. W2330 within the top plot was filtered to only capture spectra that have wavelengths
>2320 nm (W2330 dMgOH/dFeOHmask), with points coloured by dMgOH/dFeOH (≥3 equals type 1
amphibole). W2330 within the bottom plot was filtered for spectra that have wavelengths <2320 nm (W2330
D2390mask), with points coloured by D2390 (≥0.05 equals type 1 amphibole). Altogether, the red points in
the combined plots represent the complete distribution of type 1 amphibole.
22
Given the similar crystal habit and evidence for alteration of Al- and Si-amphibole (Figure 3-1), it is
reasonable to assume that all of the compositionally zoned amphibole associated with the Si-amphibole
assemblage may have originated as Al-amphibole. This, combined with the similar spectral
characteristics of both amphibole types, suggests that the crystal structure of each amphibole phase is
one and the same because spectroscopy measures the crystal lattice configuration rather than elemental
abundance. In this scenario, the only difference between phases is marked by a straight elemental
substitution that may include Mg for Fe2+
or Al for Fe3+
in C sites and Si3+
for Al in T sites, but unlike
conventional tschermakite substitution may not affect the site order and potentially change the spectral
response. If the coarse-grained and zoned Si- amphibole is an alteration feature of Al- amphibole, the
D2390-DMgOH/DFeOH index is a reliable method to detect Al-amphibole, both preserved and relict,
and in combination with indices that measure Si-amphibole assemblages (epidote, anhydrite, prehnite
and massive biotite) enables the detection of overprinting alteration zones/assemblages within the same
sample.
3.4 SIGNIFICANCE OF AMPHIBOLE - EPIDOTE - CLINOZOISITE
RELATIONS
Amphibole and epidote-clinozoisite characterization through detailed textural and compositional studies
allows for confident interpretation of large-scale mineralogical patterns derived from spectral
interpretation. The discussion below relates the microscopic-scale textures to potential large-scale
processes, which leads to the application of hornblende-tschermakite and epidote-clinozoisite as
exploration tools.
Mineralogic zonation of veins implies that variable P-T or fluid conditions were involved in the
formation of contrasting mineral phases, and based on this assertion, two scenarios may be proposed
depending on whether mineral distribution represents a replacement texture, or whether the veins grew
in a sequence of events. Certain vein textures may suggest that hornblende-tschermakite and actinolite
were replaced by clinozoisite and epidote, respectively, given that clinozoisite preferentially replaces
hornblende-tschermakite and epidote replaces actinolite, particularly as along strike within the same
vein early hornblende-actinolite zonation is post-dated by a relatively late epidote assemblage.
Alternatively, given a different set of textural examples, multiple mineral phases within veins and as
selvage to veins may equally represent sequentially layered mineral growth related to episodic pulsing
of compositionally distinct fluids through a vein during a single extensional phase. Non-syntaxial,
oriented mineral growth is typical of the initial “crack-seal” phase characterized by anisotropic and/or
competing crystal growth between neighbouring grains upon a substrate of contrasting composition
(Cox and Etheridge, 1983). In the context of Figure 3-4d, the initial “crack-seal” phase is represented
by all of the coarse, singly oriented epidote and hornblende-actinolite that would ascribe all mineral
23
growth to a single vein opening event, yet the internal amphibole zonation and the mutual overprinting
of epidote and hornblende-actinolite would suggest an episodic contribution of compositionally
different fluids during the growth increment. Most significantly, the contrasting mineralogy combined
with multiple, mutually overprinting layers of epidote and hornblende-actinolite indicates that the
proposed extension vein, as well as the vein array it is part of, were the sites of deposition for more than
one fluid type, and furthermore the preference for tschermakite and epidote to grow along separate
foliation planes suggests that the transport of fluids was partitioned between contrasting structural
elements.
The small-scale textural relationships involving the key amphibole and epidote-clinozoisite phases have
the potential to add geological context to the spectro-mineralogical distributions within km-scale 3D
models. For example, variation in epidote composition in relation to vein-matrix boundaries may point
towards the interaction between a fluid external to the vein and/or equilibration with the wallrock
(Figure 3-4d), but either way the vein-hosted epidote (+amphibole) and the more aluminous, matrix-
hosted phase may serve as a proxy for the deposit-scale proximal epidote and distal clinozoisite,
respectively (e.g. the Victory - Defiance section; chapter 4). Depending on the scale of the modelled
mineralogical data, further information on the alteration history combined with lithological and/or
metamorphic variability may be necessary to fully understand model complexities. Distinctly different
epidote and clinozoisite phases hosted within mutually overprinting veins and oscillatory-zoned grains
suggest that at least on the scale of the thin section there were fluctuating contributions from two
external fluids associated with epidote and clinozoisite end-members. Lithogeochemistry and/or
metamorphic mapping may be equally important to understand the presence of epidote-clinozoisite also.
In the case of clinozoisite, given the relatively high Al and Ca contents of some the earliest-formed
amphibole and plagioclase, respectively – compared to actinolitic and less-calcic plagioclase equivalents
– it is likely that the retrograde reaction (1) involving metamorphic hornblende and anorthite (An)
would result in the growth of clinozoisite±chlorite±quartz:
10Ca2(Mg,Fe)3Al4Si6O22(OH)2 + 4CaAl2Si2O8 + 20H2O →
hornblende anorthite
12Ca2Al3Si3O12(OH) + 3(Mg,Fe)10Al4Si6O20(OH)16 + 14SiO2 (1)
clinozoisite chlorite quartz
24
In consideration of the similar reactions resulting in both metamorphic- and alteration-derived epidote-
clinozoisite, the way to differentiate the two may lie in the spatial distribution of precursor amphibole
and plagioclase phases.
Discrimination between metamorphic- and alteration-related hornblende-tschermakite and calcic
plagioclase is important in its own right, as well as being an important factor in understanding the
occurrence of clinozoisite and epidote, as outlined in rules 1- 6 previously. The main difference
between metamorphic and alteration-related mineral phases at the deposit-scale is that variation in the
former is largely controlled by lithology whereas the latter is mainly restricted to veins and foliations.
In terms of metamorphic-related minerals, lithogeochemistry has a large role to play in identifying
anomalous rock types that would differentiate hyperspectrally classified amphiboles, but the most
effective way to separate metamorphic- from alteration-related minerals has been in the 3D modelling of
hyperspectral data. Within two independent models, a single spectral index has delineated alteration-
related hornblende-tschermakite hosted within planar structures that transect lithological boundaries
(Roache 2008). In fact, because hornblende-tschermakite was predominantly replaced by clinozoisite,
further indications of structurally hosted hornblende-tschermakite within the 3D models may come from
knowledge gained from the new epidote-clinozoisite spectral index. Therefore, there are now
mechanisms in place to effectively map hornblende-tschermakite and epidote-clinozoisite distribution at
the deposit-scale that are being captured within the Vic-Def (St Ives) and Bullant 3D models as part of
M400. Thermal infrared capability in the near future will measure plagioclase composition to further
enhance the mapping of alteration zones.
Employment of spectral indices beyond near mine applications would be more reliant upon
supplementary datasets such as whole-rock geochemistry, as interpretation of sparse, 2D spectral
information is reliant upon knowledge of lithological variation. Lithology is especially important at
large scales, because below a particular density of spectral coverage, structurally controlled alteration
would not be expressed as a linear feature – rather as a few anomalous points – even though hornblende-
tschermakite-labradorite structures may be tens of metres wide. At St Ives, similar textures to that in
Figure 3-2 have been recognized and micro-probed (Ruming, 2006) but the significance of such
alteration was not recognized, nor documented on a large scale. Three-dimensional mapping of SWIR
hyperspectral data and subsequent validation of the mineralogical parameters led to the discovery that
gold-hosting hornblende-foliated zones are laterally extensive, and that they are only mineralised where
they overlap with rock of a particular alteration type (Roache et al., in prep).
25
4 SPECTRAL MAPPING, VICTORY-DEFIANCE, ST IVES
The Victory-Defiance section (Figure 4-1) is ~ 4km in length and trends north-east across the Victory
Defiance Complex, passing south of the Victory - Defiance lodes (Leviathan open-cut). The section
includes the East Repulse lodes to east of the Victory - Defiance lodes and the Conqueror lodes to the
southwest. Work on the section during the M400 project involved interpretation of hyperspectral data
collected during the M373 and Y4*pmd*CRC projects. The aim was to:
map alteration patterns (gradients) spatially associated with Au mineralization,
validate the mineralogy, and
understand the significance of the mineralogy in terms of lithological controls and the thermo-
chemical processes driving mineralization; based on work undertaken in M358, M377 and
ongoing consultancies with St Ives Gold Mine.
Peter Neumayr (Blewett et al., 2008; Neumayr et al., 2005; Walshe and Neumayr, 2009), Kevin Ruming
(Ruming, 2006) together with Matt Crawford and Damien Keys (St Ives Gold Mining Company, pers
comm.) contributed to the development of the 3D Leapfrog® model of the Victory - Defiance Complex
used to construct the section in Figure 4-2. Figure 4-3 shows the distribution of diamond drill holes
logged hyperspectrally.
Figure 4-1: Location of Victory-Defiance section.
26
4.1 GEOLOGY
The Victory - Defiance Complex is hosted by rocks of the Kalgoorlie Sequence. In the west of the
section shown in Figure 4-2 the upward facing stratigraphic sequence (Tripod Hill Komatiite, Devon
Consols Basalt, Kapai Slate and Paringa Basalt) dips west. The sequence is disrupted in the central-east
of the section by the east dipping Repulse Thrust (Surface 1 in Figure 4-2). Above the Repulse is a unit
of the Tripod Hill Komatiite (THK), typically 10-40 metres thick and altered to talc - carbonate ±
chlorite ± amphibole. The THK is commonly overlain by Paringa Basalt and rarely by Devon Consols
Basalt (DCB) followed by Paringa Basalt. Contacts are invariably sheared and/or faulted.
Figure 4-2: Leapfrog® model of Victory-Defiance section, looking to NW.
Deposits delineated by 2gm Au shells (blue-grey). The Conqueror deposit is on the SW end of the section
and East Repulse deposit on the NE end of the section, beneath the Repulse Thrust. Ore shells for the
Victory and Defiance deposits are central &”background” in the model.
Mg- and Cr-rich lower Paringa Basalt (LPB) is differentiated from Mg- and Cr-poor upper Paringa
Basalt (UPB). The classification of upper and lower Paringa basalt is based on a camp-scale subdivision
of Paringa Basalt developed by the St Ives Gold Mine (pers. comm. Matt Briggs and Scott Halley). In
this section the UPB occurs only above the Repulse Thrust. The boundary between LPB and UPB is in
part defined by the Britannia Shear, a hanging-wall splay to the Repulse Thrust.
27
Below the Repulse Thrust the west dipping contact between the LPB and DCB is marked by Kapai Slate
and intrusions of Defiance Dolerite (Surface 2 in Figure 4-2). The contact between the DCB and THK (a
segment is shown as Surface 3 in Figure 4-2) is also generally west dipping.
The southwest dipping Surface 4 (Figure 4-2) is defined in part by a magnetite-rich siliceous and
foliated unit bounded by the DCB, as well as by Defiance Dolerite and ultramafic rocks. Occurrences
of magnetite-rich siliceous and foliated rocks are referred to as “Kapai Slate” regardless of whether they
represent an interflow sediment or a highly altered shear of similar lithological appearance to a sediment
(Neumayr et al., 2008b). Here this structural complexity in the footwall of the Repulse Thrust is referred
to as the Ruming Surface as it was defined by Kevin Ruming as part of his PhD study (Ruming, 2006).
The surface may be a thrust, that exploited the Kapai Slate to repeat and thicken the DCB in the central
part of the section.
Figure 4-3: Location of diamond holes used to construct Victory-Defiance section.
4.2 GOLD DISTRIBUTION
The two major gold deposits on the section are the Conqueror and East Repulse deposits (Figure 4-1).
In Figure 4-2, Figure 4-3 and subsequent Leapfrog® figures the ore zones are delineated by 2 gm Au
shells (grey or blue-grey in colour). The East Repulse deposit consists of two northerly trending,
shallowly south dipping shoots, beneath the Repulse Thrust and is hosted in DCB, Kapai Slate and felsic
Deposits delineated by 2gm Au
shells (blue-grey). Diamond
holes referred to in text
indicated by white boxes
28
porphyries. The main Conqueror deposit is also a northerly trending, south dipping shoot hosted by an
interval of lower Paringa Basalt between two units of Defiance Dolerite.
4.3 ALTERATION ASSEMBLAGES AND ASSEMBLAGE ZONING
Systematic variations in reduced (pyrrhotite - pyrite) and oxidized (magnetite - pyrite ± hematite) Fe-S-
O assemblages have been documented within the St Ives Camp (Neumayr et al., 2008a). Across the
Victory - Defiance Complex secondary magnetite ± pyrite occurs between the Conqueror and East
Repulse Lodes whereas pyrrhotite ± pyrite occurs outboard of these deposits to the west and east
respectively. In the vicinity of East Repulse the reduced assemblage is common above the Repulse
Thrust and the oxidized assemblage below.
Here we document lateral and vertical zoning in silicate, carbonate and sulphate (hypogene and
secondary) assemblages across the Victory - Defiance complex, using hyper-spectral logging as the
primary tool to map the distribution of the mineralogy in the mafic and ultramafic rocks, supported by
visual logging, magnetic susceptibility measurements and multi-element data used primarily to
differentiate rock types. The following vertical zoning in alteration assemblages occurs in the vicinity
of East Repulse over a depth interval of ~350 to 400 m (Figure 4-4).
Reduced
1. Clinozoisite – chlorite ± pyrite ± pyrrhotite (top)
Transitional
2. Amphibole – chlorite (in part a background metamorphic assemblage)
3. Amphibole ± feldspar
4. Biotite ± amphibole ± albite ± pyrite ± gold
Oxidized
5. Magnetite - quartz ± pyrite ± albite (Kapai Slate) ± gold
6. Epidote ± magnetite ± pyrite
7. Anhydrite ± phlogopite (bottom)
These assemblages are classified as reduced, oxidized or transitional/mixed reduced-oxidized
assemblages. The first named mineral is considered the characteristic mineral of the assemblage but it is
not necessarily the most abundant. Carbonate and quartz occur in all assemblages. With minor
modification this classification scheme can be applied across the complex. In the East Repulse lodes, Au
is hosted in assemblages 4 and 5 (Kapai Slate) as well albitized porphyries.
29
Figure 4-4: Leapfrog® model showing vertical alteration zoning at East Repulse.
Figure 4-5: CD5026 Distribution of chlorite, amphibole, talc and dark micas.
A: Mg No (100mMg/(mMg+mFe)) vs depth, microprobe analyses from (Bil, 2010) B: TSG® histogram of
minerals/mineral groups. Talc is classified as “Other MgOH”.
30
Figure 4-6: Leapfrog® model showing distribution of clinozoisite - epidote.
Distribution defined by variation in the 1550 nm SWIR absorption band(warm colours clinozoisite; cool
colours epidote). Gold mineralization (2gm Au shells in blue-grey) occurs on the transition from clinozoisite
to epidote. Infrared measurements using CSIRO Hychips.
Boundaries between assemblages are commonly marked by structural ± lithological breaks. Talc ±
carbonate occurs as a background metamorphic assemblage in the THK and assemblage 2 (amphibole –
chlorite) is in part a background metamorphic assemblage in the Paringa Basalt. A comparison of the
distribution of chlorite, amphiboles (hornblende, actinolite) and dark micas (biotite, phlogopite) in
CD5026, as determined from spectral logging (TSA analysis), and the distribution and composition of
these minerals as determined by microprobe analysis (Bil, 2010) is given in Figure 4-5. The trend of
increasing Mg No of the Fe-Mg silicates, down the drill hole, follows the increasing Mg-rich nature of
the lithologies. In general there is a good match between the observed minerals (from petrography and
microprobe analysis) and the spectrally determined mineralogy. However, the more Fe-rich biotite in
the top 100 - 200m interval of CD5026 was not logged spectrally. Figure 4-6 illustrates the zoning of
clinozoisite [Ca2Al3Si3O12(OH)]) and epidote [Ca2Fe3+
Al2Si3O12(OH)]) assemblages across the Victory
- Defiance Complex, with the epidote ± magnetite assemblage focused in the core of the complex,
zoning laterally and vertically to the clinozoisite assemblage. Both the Conqueror and East Repulse
Lodes occur on the transition between clinozoisite and epidote assemblages that is equivalent to the
transition from reduced to oxidized Fe-S-O assemblages (Neumayr et al., 2008a). Epidote forms in
more oxidized environments and clinozoisite in more reduced and acidic viz:
2Ca2Al3Si3O12(OH) +3SiO2 +3Fe2+
+ 2Ca2+
+ 5.5H2O + 0.75O2 = 3Ca2Fe3+
Al2Si3O12(OH) + 10H+
Clinozoisite Epidote
31
Figure 4-7: Distribution of epidote and magnetite in CD6800.
Epidote is preferentially developed in the DCB and the major zone of epidote is in the immediate footwall of
“stratigraphic” Kapai Slate as defined from the 3D model. Epidote-clinozoisite (1550 nm band). Epidote:
less than 1550nm; Clinozoisite: greater than 1550 nm. Dashed boxes highlight magnetite-rich domains.
Figure 4-8: Leapfrog® model looking ~NNW showing distribution of anhydrite/gypsum.
Distribution defined by variation the depth of the 1750 nm absorption band. Anhydrite or gypsum pseudo-
morphs occur at depth in the section (below ~ 300m). Anhydrite is well developed beneath the East Repulse
lodes, east of the Conqueror lodes and as a broad zone about the level of the Ruming surface in the model.
Azimuth of model: 342°.
The epidote assemblage within the core of the complex is preferentially developed within the Devon
Consols Basalt (Figure 4-7). It is spatially associated with magnetite-rich Kapai Slate and is well
32
developed within the DCB in the footwall to “stratigraphic” Kapai. Hydrothermal magnetite also occurs
within the epidote assemblage as veinlets and disseminations.
The distribution of anhydrite ± gypsum is shown in Figure 4-8. Primary anhydrite occurs below ~ 300-
350m in the section, beneath the East Repulse lodes, east of the Conqueror lodes and as a broad zone
about the level of the Ruming surface. Some anhydrite veins are completely or partially pseudo-
morphed by gypsum and coarsely crystalline gypsum veins of secondary origin are most common in the
upper parts of the section. Primary anhydrite veins may have a reaction selvage of tremolite and veining
in the THK is commonly associated with narrow irregular domains of biotite alteration. Discrete
domains of phlogopite - anhydrite occur down section (e.g. CD7068; Figure 4-9) and illustrate the
association of the two minerals, although anhydrite may occur within the epidote assemblage and
phlogopite (biotite) is more extensive than anhydrite.
Figure 4-9: CD7068: Oxidized mineral assemblages.
A: Gold grades (ppm) B: Magnetic susceptibility measurements C: Epidote-clinozoisite (1550 nm band).
Epidote: less than 1552nm; Clinozoisite: greater than 1552 nm. D: Phlogopite – TSA determination E:
Anhydrite – TSA determination. Dashed boxes highlight the domains of well developed phlogopite and
anhydrite that includes a Au zone at 270 to 285m depth. Lithology code as in Figure 4-7.
In the reduced assemblage 1 in the Paringa Basalt above the Repulse Fault, coarse-grained clinozoisite
is commonly associated with irregularly shaped quartz ± carbonate veins in strongly chloritized rocks.
Feldspar occurs in the transitional assemblages. Albite is abundant in the Au zones (assemblage 4)
beneath the Repulse Fault but also occurs with biotite and carbonate above the Fault and the THK as
33
fabric preserving replacement of sheared LPB. Coarse white feldspar occurs within amphibole – rich
fabric domains at the base of the THK that define the Repulse Fault. These “veins” and accumulations
possibly replace quartz veins. This amphibole assemblage (3) typically overprints the talc - carbonate
assemblage of the THK and may overprint an earlier biotite alteration of the talc - carbonate
assemblage.
Figure 4-10: Summary of mineral paragenesis relative to timing of gold deposition.
4.4 PARAGENETIC RELATIONS
The relative timing of the alteration minerals with respect to gold deposition is summarized in Figure
4-10. The paragenetic scheme classifies minerals/mineral assemblages as pre-, syn- or post-main stage
of gold deposition (Petersen et al., 2005). The oxidized epidote ± magnetite assemblages are
paragenetically early although late cross-cutting steep veins of epidote imply the mineral was stable at
later stages of the paragenesis. The anhydrite-phlogopite assemblage commonly overprints epidote -
magnetite assemblages. Biotite associated with K-metasomatism in the transitional assemblages may
predate or overprint the amphibole - feldspar assemblage but a coarse-grained, un-orientated amphibole
also overprints the biotitic fabric in this domain. Pyrite is the common phase in the transitional
assemblage. Magnetite in the Kapai slate is overprinted by pyrite but magnetite ± hematite persists as a
minor phase, commonly as inclusions in pyrite (Neumayr et al., 2008a). Barite also occurs as inclusions
34
in pyrite in gold zones. Detailed studies of the epidote - clinozoisite relations (2.2) show a complex
relationship. Epidote may replace clinozoisite or vice-versa or there may be a continuum of
compositions between the two minerals. Biotite overprints chlorite as irregular veinlets and flecking
within the chlorite fabric but equally chlorite may overprint biotite. Minor pyrite and pyrrhotite occur in
reduced assemblages, particularly in domains with biotite. Pyrrhotite is commonly overprinted by
pyrite.
4.5 CORRELATION OF SPECTRAL CHARACTERISTICS WITH STABLE
ISOTOPES: CONSTRAINTS ON REDOX CONDITIONS
δ13
C of carbonate and δ34
S of sulfide and sulphate are sensitive indicators of redox variations in
mineralising systems. Close to the H2CO3-CH4 buffer (i.e. H2CO3 ~ CH4) the ratio of 13
C to 12
C in
carbonate changes significantly. Similarly the ratio of 34
S to 32
S is sensitive to the oxidation state of
fluids close to the H2S - SO4 buffer (i.e. SO2/SO42-
~ H2S ). Combining C and S isotope systems it is
possible to determine the highly oxidizing parts of the system (SO2/SO42-
and CO2 the dominant fluid
species), the highly reduced parts of the system (H2 ± CH4 the dominant species) and the transitions
between these extremes.
Assuming a dominant carbon reservoir with δ13
C ~ -5 to -6 ‰ and a dominant sulphur reservoir with
δ34
S ~ 0 ‰ (Walshe and Neumayr, 2009; Walshe et al., 2006) then:
1. Highly reduced domains in which H2 is the dominant reductant are defined by δ13
C carbonate
values > > -5 to -6 ‰ and δ34
S sulphide values > 0 ‰. In these domains oxidized carbon and
sulfur species (SO2, SO42-
H2CO3, CO2, carbonate) are reduced viz:
CO2 + 4H2 → CH4 + 2H2O and SO2 + 3H2 → H2S + 2H2O
2. Highly oxidized domains in which SO2/SO42-
are the dominant oxidants are defined by δ34
S
sulphide values << 0 ‰ and δ13
C carbonate values < -5 to -6 ‰. In these domains CH4 is
oxidized by SO2 or sulfate viz:
e.g. 3CH4 + 4SO2 → 3CO2 + 2H2O + 4H2S
35
Figure 4-11: δ34Spyrite across Victory - Defiance section.
Red less than -5‰ δ34Spyrite, blue greater than +3 ‰ δ34Spyrite.
Figure 4-12: δ13Ccarbonate across Victory - Defiance section.
Red - orange less than ~ -6 ‰ δ13C carbonate, blue greater than ~ -2 ‰ δ13C carbonate.
36
The most negative values δ34
S sulphide and δ13
C carbonate are focused in the central part of the Victory
- Defiance section, particularly around East Repulse (Figure 4-11 and Figure 4-12), consistent with the
mineralogical evidence that this part of the system was a highly oxidized domain in which CH4 was
oxidized by SO2 or sulphate. The pronounced shift to δ13
C carbonate values > -2 ‰ and δ34
S sulphide
values > 0 ‰ into the hangingwall of the Repulse Fault indicates a shift to highly reducing conditions in
which oxidized carbon and sulfur species (SO2, SO42-
H2CO3, CO2, carbonate) were reduced by a H2-
rich fluid. The immediate hangingwall of the Britannia Shear appears to have been the focus of this H2-
flux.
Comparison of the spectral and stable isotopic characteristics shows that there are systematic changes in
the spectral and stable isotopic characteristics of the vertical transition from the reduced assemblages
(assemblage 1) in the hangingwall of the East Repulse mineralization through to the oxidized
assemblages in the footwall (assemblage 5, 6 and 7).
In CD5026 the reduced assemblage occurs within the UPB (Figure 4-13) in the hangingwall of the
Britannia shear. The distribution of clinozoisite [Ca2Al3Si3O12(OH)]) versus epidote
[Ca2FeAl2Si3O12(OH)]) in the hole is indicated by the variation of the SWIR band at 1550 nm. Values
greater than 1550 nm, that are indicative of clinozoisite, mostly occur within the UPB. δ13
C of carbonate
within this interval mostly exceeds 0 ‰ and δ34
S of both pyrite and pyrrhotite are also positive,
consistent with a highly reduced domain in which H2 was the dominant reductant.
In contrast the epidote in CD5026 occurs within the DCB below the upper unit of THK broadly
associated with phlogopite. δ13
C carbonate values within this interval are mostly < -5 ‰ and δ34
S pyrite
between 0 and -10 ‰, consistent with oxidising conditions. Within the oxidized zone, between ~ 273
and 313 m, values of δ18
O carbonate vary between ~ 10 to 20 ‰ indicative of switching between the 1-
phase and 2-phase fluid domains (Walshe and Neumayr, 2009).
A similar correlation between the distribution of clinozoisite - epidote, biotite and values of δ13
C
carbonate and δ34
S pyrite and pyrrhotite is observed in CD4997 (Figure 4-14) and provides evidence of
a zone of reduction in the hangingwall of the Repulse Fault. This zone is laterally extensive across the
top of the Victory - Defiance Complex as mapped by the distribution of the clinozoisite (Figure 4-6).
Mg-chlorite ± amphibole, as mapped by the depth of 2385 nm band, is variably distributed within the
oxidized domain and occurs transitionally between the reduced and oxidized domains. The assemblage
occurs in both the DCB and the LPB and to a lesser extent in the THK and UPB. Mg-chlorite ±
amphibole is particularly well developed in CD6024 (Figure 4-15) in the transitional redox zone above
the THK, compared with CD5026 and CD4997. These patterns suggest it may be possible to use the
distribution of this assemblage with respect to clinozoisite in the hangingwall to aid the identification of
centres of oxidation in the footwall.
37
Figure 4-13: Spectral and isotopic properties of CD5026.
Top Panel: A: Magnetic susceptibility measurements B: Gold grades (ppm) C: Variation of 2330 nm (Mg-
OH) SWIR band D: Depth of Mg-chlorite/amphibole band (2385 nm SWIR band); E: Epidote-clinozoisite
(1550 nm band). Epidote: less than 1552nm; Clinozoisite: greater than 1552 nm. F: Phlogopite – TSA
determination.
Lower Panel: A: Magnetic susceptibility measurements B: Gold grades (ppm) C: δ34S pyrite and pyrrhotite
(‰) D: δ13Ccarbonate E: δ18O carbonate.
Lithology code as for Figure 4-7.
38
Figure 4-14: Spectral and isotopic properties of CD4997.
Panels as for Figure 4-13.
39
Figure 4-15: Spectral and isotopic properties of CD6024.
Panels as for Figure 4-13.
40
4.6 SUMMARY
Correlations between stable isotopic characteristics and silicate mineralogy, as mapped by SWIR
hylogger/hychipper technologies, confirm that systematic changes in the silicate alteration mineralogy
reflect changes in the redox state of Late Archean Au systems.
In general terms:
Clinozoisite - chlorite ± pyrite ± pyrrhotite assemblages reflect reduced conditions
Epidote ± magnetite ± pyrite and anhydrite ± phlogopite assemblages reflect oxidized
conditions
Amphibole ± phlogopite ± phlogopite reflect transitional reduced – oxidized conditions.
Mutually overprinting paragenetic relationships between clinozoisite and epidote as well as biotite,
amphibole and chlorite suggest that the development of the reduced and oxidized assemblages
overlapped in time.
These redox changes are spatially related to gold occurrences.
Both the mineralogical and isotopic patterns provide opportunities to map from barren to productive
parts of Au systems. In particular these systematic changes offer the possibility of recognising the
likely location of deposits at depth. Zoning from reduced and acidic to oxidized/neutral alkaline mineral
assemblages, coupled with positive to negative switches in δ13
C of carbonate and δ34
S of sulphide, are
indicative of productive gradients.
41
5 SPECTRAL AND STABLE ISOTOPE STUDY, WALLABY
DEPOSIT, LAVERTON
5.1 GEOLOGICAL SETTING
The Wallaby deposit is hosted by conglomerates of the Wallaby basin, a late Archean sedimentary basin
preserved on the periphery of the Mount Margaret Dome (Figure 5-1). Gravity data shows that the
Mount Margaret Dome that lies northwest of the deposit is cored by a large granite intrusion. The
Wallaby basin is interpreted as the last of three separate basins that overlie the Mount Margaret Dome
complex (Walshe et al., 2006). The basins and mafic substrate were subsequently thrust stacked. The
Thet’s Fault (Figure 5-1; left panel) marks the contact between the Wallaby basin and middle basin that
is dominated by a conglomerate facies. Beneath the Slaughteryard Fault, the lower basin has a thick
sequence of black, reduced turbidites, coarsening downwards to a basal sequence of conglomerates.
Figure 5-1: Wallaby deposit and environs.
Left panel: Geological map of Laverton district around the Wallaby deposit. Right panel: Leapfrog® model
of Wallaby pipe. A: Looking west, Yellow:1 gram isotropic Au shell, White: Model of magnetic susceptibility
(> ~ 3000*10-5SI ). B: Plan view, at plunge of 78° to west, through 20m section of magnetic susceptibility
shells. Yellow: 3 gram isotropic Au shell.
42
The Wallaby Au deposit (Mueller et al., 2008; Salier et al., 2004) occurs within a pipe-shaped zone of
amphibole-magnetite-epidote-calcite (AMEC) alteration centred on a NE trending swarm of monzonite
and monzodiorite porphyries and later syenite dykes. Sub-horizontal Au lodes are associated with
carbonate-albite-quartz-pyrite ± biotite ± magnetite alteration. District-scale alteration surrounding the
Wallaby pipe that is clearly visible in the regional magnetic image (Figure 5-2) appears to be
asymmetrically zoned. To the northeast there is an extensive zone of magnetite known as the Wallaby
tail. The SWIR wavelength for white mica through this zone and also in a broad zone to the northwest is
indicative of muscovite - paragonite (SWIR less than 2195 nm; Figure 5-3). Both the Thet’s Fault and
Slaughteryard Shear have intense alteration of paragonite - ankerite - pyrite ± chloritoid - pyrrhotite
alteration developed along them. The combination of paragonite ± chloritoid ± pyrrhotite is indicative of
reduced and acidic fluids. The same alteration assemblage is seen on the north-south faults like
Chatterbox and Shocker, in the Lancefield conglomerate above the Lancefield deposit, and in the
conglomerate basin south of Mount Margaret, indicating a widespread distribution of the reduced and
acidic fluid.
In contrast the composition of white micas immediately surrounding Wallaby deposit and notable to the
southwest is muscovitic to phengitic (SWIR greater than 2200 nm; Figure 5-3) is quite different to the
alteration signature associated with Thet’s Fault, reflecting a more alkaline fluid composition in this
environment. The muscovitic to phengitic mica also corresponds with a zone of elevated W-Mo-Bi, in
contrast to the As-Sb signature of the more acid-reduced domain.
Figure 5-2: Magnetic map of the Wallaby deposit and environs.
43
Figure 5-3: Paragonite, muscovite & phengite distribution in the Wallaby hinterland.
Composition as measured by the wavelength of the 2200nm feature using PIMA (Walshe et al., 2006).
The differentiated dyke suite of the Wallaby deposit occurs as two main shoots plunging 50 to the
south and extending to >1km in depth. The dykes range in composition from relatively early monzonite
and carbonatite through younger syenite and porphyritic syenite (Drieberg et al., 2004). Both pre-ore
and post-ore lamprophyre dykes are also present. An alteration assemblage of magnetite - actinolite
(AMTA) epidote pyrite forms a pipe-like body mantling the syenite dyke suite (Wall and Mason,
2001). The actinolite-magnetite alteration occurs as groundmass alteration of basaltic clasts and along
thin discontinuous fractures in the meta-conglomerates. Early intrusions such as monzonite and
carbonatite are overprinted by the actinolite – magnetite assemblage but younger intrusions of syenite
and porphyritic are not overprinted (Drieberg et al., 2004). In plan-view the distribution of magnetite in
the Wallaby deposit is U-shaped and open to the west (Figure 5-1; right panel), suggesting it is
controlled by E-W and N-S trending structures, the latter possibly related to the Chatterbox Fault. Veins
of calcite-feldspar-biotite-pyrite-magnetite (“magmatic carbonate veins”) intrude syenite porphyry with
biotite overprinting 10cm of the contact (Dreiberg, unpublished PowerPoint presentation). A later
hematized syenite dyke crosscuts the magmatic carbonate vein, linking these veins to the emplacement
of the syenite and porphyritic syenite. The veins are associated with red biotite–sericite–calcite–albite
alteration in earlier monzonite dikes (Mueller et al., 2008). Brecciated fragments of altered (dol-ab-py)
conglomerate within syenite (Dreiberg, unpublished PowerPoint presentation) also indicate alteration
44
was initiated pre/syn-emplacement of the syenite. Structural relations and a concordant titanite U–Pb
age constrain this stage of intrusion and mineralization to 2,662±3 Ma (Mueller et al., 2008).
Gold mineralization is wholly contained within the actinolite-magnetite alteration pipe and occurs as a
series of flat-lying ore lodes linked by small, steep, high-grade ore lenses, some of which appear
controlled by the intersection of N-S and E-W structures (Figure 5-1; right panel). A characteristic
intense “bleaching” alteration (ASRC) associated with the major high-grade gold event is composed of
albite, ferroan dolomite and pyrite with abundant quartz-carbonate veins. This alteration may be
asymmetric with one sharp contact and a diffuse contact grading into an earlier assemblage of quartz,
Fe-rich dolomite, hematite, pyrite (ASRH) with low grade Au (up to 2.5 gms). High grade gold lodes
and intense alteration occur where extensional quartz-carbonate veins link with laminated quartz-albite
veins. Flat-lying quartz-carbonate breccias may be associated with high grade Au zones.
Changes in the observed alteration assemblages and styles of mineralization may be linked to a series of
palaeo-stress switches (Miller, 2005):
Emplacement of alkaline intrusions marks a stress switch from E-W shortening (D2 folding
event) to radial extension. The syenite dykes and magmatic calcite veins have variable strikes,
but intersect at a point plunging 60° S that matches the plunge of the larger intrusive bodies.
A N-directed shearing event occurred at the end-stage of magmatism that marks a stress switch
from extension to compression. This folded syenite dykes with substantial flattening of
conglomerate clasts and chloritization of magnetite-actinolite alteration. Many of the N-
directed ductile shears preferentially localised along SE-dipping bedding surfaces within the
Wallaby conglomerate.
The first major phase of gold mineralization, linked to hematite-associated alteration within
predominantly brittle structures, formed during N-S and NW-SE compression. A switch to
extension marks the end of hematite-associated deformation.
A phase of sinistral-slip faulting (transport direction of top-to-NW and –N) is related to major
gold mineralization (termed sinistral-slip lodes) that overprints the hematite-associated lodes.
The lodes formed when σ1 was sub-horizontal and oriented NW-SE and σ2 plunging 30 to 40°
NE.
Xenotime and monazite U-Pb ages of 2,650±6 Ma from altered wall rocks / quartz matrix breccias
constrain the late stage of high-grade gold (Salier et al., 2004). A single molybdenite Re–Os age of
2,661±10 Ma (Mueller et al., 2008), from pyrite-rich, hematite-stained, sericite–dolomite–albite
replacement ore (8.1 ppm Au) in the deep central part of the Wallaby deposit, may be the best estimate
45
of the age of the hematite-associated gold event. The uncertainty of these ages remains significant. A
summary of the relative timing of events is given in Figure 5-4.
Figure 5-4: Relative timing of magmatic, deformation and alteration events.
Figure 5-5: Biotite to dolomite - albite - pyrite zoning.
5.2 ALTERATION ZONING IN THE WALLABY DEPOSIT
Dreiberg (unpublished PowerPoint presentation) showed that at least locally around the Au lodes there
is a zonation from biotite /carbonate - biotite shears through carbonate - magnetite through to dolomite -
albite - pyrite (ASRC assemblage) with pyrite replacing magnetite (Figure 5-5). The outer biotite–
sericite alteration zones are very dark brown to black in colour, are tens of centimetres to metres wide,
and are composed of biotite + sericite + minor pyrite + magnetite ± rutile ± zoisite ± chalcopyrite
46
Figure 5-6: View of SWIR & isotope data in Leapfrog® model, upper section Wallaby deposit.
A: Phlogopite _TSA interpretation. B: Anhydrite; depth of 1945nm SWIR band C: Amphibole from depth of
2385 nm SWIR band D: Amphibole from depth of 2330 nm SWIR band E: Clinozoisite (blue) – epidote
(red) 1550 nm SWIR band F: FeOH wavelength (2250); cool colours - Fe rich, warm colours Mg-rich . G:
δ34Spy warm colours - negative values, cool colours – positive values H: δ13Ccarb warm colours - negative
values, cool colours – positive values. Grey shells: >1 gm Au 1= WB0101AD 2= WB0096AD 3= WB0090AD
4= WB0172AD 5=WB0801CD. Section looks west.
47
Figure 5-7: Location, lithology and alteration zoning of WB801CD.
A: Leapfrog ® model looking west of magnetic susceptibility (red shell > ~3000*10-5SI ) with SWIR 2200 nm
band for phengite (warm colours) through muscovite to paragonite (cool colours). B: 1gram Au shell
(isotropic model) with SWIR 2200 nm band. C. SWIR FeOH (2250nm) band; cool colours - Fe rich
(2260nm), warm colours Mg-rich (2248nm) D. Summary log of lithology and alteration.
(Wall and Mason, 2001). Fine-grained biotite (brown) has severely replaced actinolite and plagioclase
of precursor actinolite–magnetite alteration in texture-destructive manner. Where lodes taper along
48
strike of the controlling fault, inner sericite–dolomite replacement is surrounded by 10–20-cm-thick
outer zones of dark brown biotite–calcite alteration (Mueller et al., 2008), marked by minor albite,
chlorite, the assemblage magnetite + pyrite (5–10%), and trace chalcopyrite. Where the alteration
envelope closes, the fault plane is lined with thin quartz–carbonate veins in contact with conglomerate-
hosted skarn.
The hyperspectral data acquired during the M373 and M377 projects and summarized in Figure 5-6
provide evidence of an equivalent zoning at a larger scale. Figure 5-6A shows a zone of phlogopite
enrichment subjacent to gold zones. Anhydrite (Figure 5-6B) and epidote (Figure 5-6E) occur outboard
of the phlogopite zone and amphibole is transitional (Figure 5-6C&D). The stable isotopes
(δ13
Ccarbonate & δ34
Spyrite) are zoned from negative to positive (red to blue; Figure 5-6G&H) into the
phlogopite domain. These data imply a spatial as well as temporal evolution in the Wallaby mineral
system that is yet to be defined.
5.3 WALLABY WB0801CD
WB0801CD provided an opportunity to study the transition from proximal alteration associated with the
northern lodes of the deposit through to distal alteration of the late basin sediments. The Wallaby
Conglomerate extends to ~ 800 m in WB0801CD becoming increasing deformed with depth (Figure
5-7). Highly deformed basaltic rocks occur above Thet’s Fault. Below Thet’s Fault conglomerate
transitions downward to grits, conglomerates and basalt with bedded turbidites occurring below the
Slaughteryard Fault. The summary of alteration assemblages in Figure 5-7 is based on SWIR spectral
logging at 1m intervals and the summary of the spectral interpretations is given in Figure 5-8 through
Figure 5-10 along with magnetic susceptibility measurements, gold grades and stable isotope data (δ13
C,
δ18
O carbonate and δ34
S of sulfide and sulphate).
Integrating these data the alteration assemblages may be broadly subdivided into oxidized and neutral-
alkaline (O-NA) assemblages or transitional assemblages in the upper ~ 600m of WB0801CD within the
Wallaby Conglomerate. In contrast reduced and acidic assemblages (R-A) occur below ~ 800m within
the deformation zone related to the Thet’s and Slaughteryard Faults.
O-NA Assemblages: Phlogopite/anhydrite ± amphibole ± epidote ± magnetite
Epidote ± magnetite ±phlogopite ± phengite ± chlorite
Transitional: Chlorite ± amphibole ± magnetite
Muscovite/phengite ± chlorite
R-A Assemblages: Muscovite/paragonite
Chloritoid/muscovite/paragonite
49
Figure 5-8: WB0801CD oxidized alteration assemblages.
Panels: A: Gold grades (ppm) B: Magnetic susceptibility measurements C: Epidote - depth of 1550nm SWIR
feature. D: Phlogopite – TSA determination E: Anhydrite - pfit depth of 1944 feature F: Variation of 2250
nm (Fe-OH) band G: δ34S anhydrite, pyrite and pyrrhotite.
Figure 5-9: WB0801CD reduced and acid alteration assemblages.
Panels: A: Log gold grades B: Magnetic susceptibility measurements C: Distribution of chloritoid - 1495nm
SWIR band D: 2200 nm SWIR band - 2190-2195 paragonite, 21905-2210 muscovite, > 2210 phengite E:
Depth of 2330nm band F: Depth of 2385 nm SWIR band – amphibole/ Mg-chlorite G: δ13C carbonate.
The alteration in the Wallaby Conglomerate at less than ~ 700m depth in WB801CD forms part of the
amphibole - magnetite - epidote - calcite (AMEC) alteration of the Wallaby pipe. In detail the
paragenesis of this zone is complex. Magnetite and epidote coexist down to Thet’s Fault at 1050m,
although most occurs above 700 m, with the epidote occurring as a late fracture-controlled over-print.
Amphibole within undeformed mafic clasts in the upper part of the hole is altered by epidote, carbonate
and rutile (Figure 5-11). Calcite veins are relatively common in the upper hole and more rarely rounded
carbonate pebbles occur – possibly after quartzite pebbles. Rounded quartzite pebbles occur below at
400m. Zones of phlogopite alteration above ~ 700m are partly centred on porphyries and spatially
associated with anhydrite, particularly in the interval from ~50 to 125m. Biotite veinlets and folia form
50
after amphibole and epidote and replace porphyry phenocrysts. Conversely amphibole overprints biotite
and epidote in narrow shears.
Figure 5-10: WB0801CD comparison of gold grades with stable isotopes.
Panels: A: Gold grades (ppm) B:δ34S anhydrite, pyrite and pyrrhotite C: δ13C carbonate D: δ18O carbonate
E: Magnetic susceptibility measurements.
Figure 5-11: Photomicrographs of epidote replacement of hornblende F.O.V = 1.5x1mm.
Sample WB0801CD 116 m. a) Plane-polarized transmitted light photomicrograph of unaltered hornblende
(Hb) and hornblende partially-altered to epidote (Ep). Areas of most intense epidote alteration are denoted
by a deep apple-green colour. b) Cross-polarized transmitted light photomicrograph of the same area as in
Figure 1a. The epidote-altered hornblende grain in the upper right of the image has birefringence colours
that reflect the epidote colouration seen in Figure 1a; partially-altered hornblende has second order colours,
whereas epidote is characterized by relatively high order colours, approaching third order.
Deformation progressively increases downwards in WB0801CD to Thet’s Fault, obliterating the
conglomeratic texture of the chlorite–calcite altered meta-conglomerates and producing a strongly
foliated rock with highly elongated altered lithic fragments. A similar progression occurs in
51
WB0223ADW1 and WB0211AD (Wall and Mason, 2001). Alteration assemblages are dominated by
white mica, carbonate, chlorite, quartz, sulphides (pyrrhotite, pyrite, chalcopyrite), magnetite,
tourmaline and ilmenite. The presence of deformed bleached domains (pinkish brown carbonate-rich
zones) within highly foliated rocks demonstrates that the alteration / deformation in the fault post-dates
the onset of mineralization and alteration (Miller, 2005), reflecting a N-directed shearing event.
A chloritoid ± paragonite ± muscovite assemblage in WB0801CD occurs immediately below Thet’s
Fault within a broader zone of paragonite ± muscovite that extends from above Thet’s fault down to the
Slaughteryard Shear. The distribution of chloritoid is denoted by the 1495 nm SWIR band and
paragonite ± muscovite by SWIR band less than ~ 2195 nm (Figure 5-9). Chloritoid is predominantly
restricted to intensely developed white mica ± chlorite foliations. Its occurrence coincides with a quiet
zone in magnetic susceptibility and marks the transition from pyrite to pyrite ± pyrrhotite at greater
depth. Chloritoid forms dark green twinned prismatic crystals overprinting a foliated white-mica
(muscovite-paragonite?) matrix. These observations confirm that the late shear zones were accompanied
by high strain and modification of the precursor metabasaltic conglomerate alteration assemblages.
Amphibole is concentrated along plagioclase + quartz-bearing vein margins that are enveloped by the
foliation mentioned above, the amphibole being replaced by chlorite.
Gold-rich zones occur in the upper 700 m of WB0801CD within the O-NA assemblages and transitional
assemblages. Typically gold rich zones are associated with albite-dolomite-calcite-pyrite alteration.
Anomalous gold concentrations (~ 0.1 to 0.2 gms Au) are associated with the chloritoid zone at 1075 to
1100m (Figure 5-9).
5.4 STABLE ISOTOPES, MINERAL ASSEMBLAGES & SPECTRAL
CHARACTERISTICS: CONSTRAINTS ON REDOX CONDITIONS
The variation of δ34
Spyrite, δ13
Ccarbonate and δ18
Ocarbonate as a function of alteration assemblage,
paragenetic stage and Au grade stages for the Wallaby deposit is summarized in Figure 5-12 through
Figure 5-14. There is a general trend of increasing δ34
Spyrite from dominantly negative values in the
early CC_Bi_MT (calcite-biotite-magnetite) and AMTA (magnetite - amphibole ± epidote ± calcite ±
biotite) veins ±assemblages through to dominantly positive values in the ACCH (calcite - chlorite) and
reduced/acid (paragonite - muscovite - chloritoid) alteration associated with the ductile deformation
52
Figure 5-12: Variation of δ34Spyrite through paragenetic stages of the Wallaby deposit.
Paragenesis as defined in Figure 5-4
CC_Bi_MT: Early calcite-biotite-magnetite veins (“magmatic calcite veins”)
AMTA: Magnetite-amphibole±epidote±calcite±biotite mantling syenite dykes
ACCH: Chlorite-calcite veins/alteration overprinting AMTA
Reduced-acid alteration: Paragonite-muscovite-chloritoid
Hm associated lodes: Quartz-carbonate-muscovite-albite-hematite
Sinistral-slip lodes: Quartz-carbonate-muscovite-albite-pyrite-fuchsite.
53
Figure 5-13: δ13Ccarbonate vs δ18Ocarbonate for the Wallaby deposit.
Top panel: Isotopic variation as a function of alteration assemblage/paragenetic stage.
Lower Panel: Isotopic variation as a function of Au grade.
54
Figure 5-14: δ13Ccarbonate vs δ34Spyrite for the Wallaby deposit.
Top panel: Isotopic variation as a function of alteration assemblage/paragenetic stage.
Lower Panel: Isotopic variation as a function of Au grade.
55
event. The hematite associated Au lodes show a spread in δ34
Spyrite values with a significant negative
component. In contrast values are dominantly positive for the assemblages of the sinistral slip lodes
(quartz - carbonate - muscovite - albite - pyrite - fuchsite). δ13
Ccarbonate values of the early CC_Bi_MT
assemblages are mostly less than ~ -4 ‰. AMTA carbonates show a spread of values (~ -6 to +2 ‰)
transitional to the δ13
Ccarbonate values of the ACCH and reduced/acidic alteration assemblages that
range from ~ -7 to +3 ‰ with most values greater than -4 ‰. δ18
Ocarbonate show corresponding shifts
with δ18
O values from early CC_Bi_MT and AMTA assemblages mostly less than 15 ‰ transitional to
δ18
O values between ~13 and 18 ‰ for the later ACCH and reduced/acidic alteration assemblages.
High grade Au samples (10 to ~ 100 gms Au) show a very narrow range in δ13
Ccarbonate (-3 to -4‰),
a wide but elevated range in δ18
Ocarbonate values (~13 to 23 ‰) and mostly positive values of
δ34
Spyrite (~0 to 23 ‰). Au samples with 1-10 gms grade overlap this isotopic range but are transitional
to more negative δ13
Ccarbonate and δ34
Spyrite values and lower δ18
Ocarbonate values.
δ13
Ccarbonate and δ34
Ssulfide and sulphate are sensitive indicators of redox variations in mineralising
systems. Close to the H2CO3-CH4 buffer (i.e. H2CO3 ~ CH4) the ratio of 13
C to 12
C in carbonate changes
significantly. Similarly the ratio of 34
S to 32
S is sensitive to the oxidation state of fluids close to the H2S
- SO4 buffer (i.e. SO2/SO42-
~ H2S ). Combining the C and S isotopic systems it is possible to determine
the dominant oxidised and reduced COHS-species present in fluid(s) that co-existed with the carbonate,
sulphides and sulphate, assuming one dominant carbon and one dominant sulphur reservoir (Walshe and
Neumayr, 2009; Walshe et al., 2006). Figure 5-15 illustrates the inferred speciation as a function of
δ13
Ccarbonate and δ34
S pyrite.
Figure 5-15: Inferred COH speciation from δ13C carbonate and δ34S pyrite.
The interpretation assumes a
dominant carbon reservoir of
δ13
C ~ -5 to -6 ‰ and a dominant
sulphur reservoir of δ34
S ~ 0 ‰
56
Negative values of δ34
S pyrite in combination with δ13
Ccarbonate less than ~ -6 ‰ define domains in
which the concentration of oxidized sulphur species, such as SO2 or SO42-
, in the fluids exceeded
reduced sulphur species. CH4 was oxidized to CO2 via
3CH4 + 4SO2 → 3CO2 + 2H2O + 4H2S with SO2 >> CH4
Conversely, domains of δ34
S sulphide > 0 ‰ in combination with δ13
Ccarbonate less than ~ -6 ‰
define conditions where reduced species (CH4, H2) were dominant and SO2 ± SO42 were reduced viz:
SO2 + 3H2 → H2S + 2H2O with H2 >>SO2
or
3CH4 + 4SO2 → 3CO2 + 2H2O + 4H2S with CH4 >>SO2
Domains of δ13
C carbonate values > > -4 to -5 ‰ and δ34
S sulphide values > 0 ‰ imply highly reducing
conditions with H2 the dominant reductant. Oxidized carbon species (H2CO3, CO2, carbonate) are
reduced as well as oxidized sulphur species viz:
CO2 + 4H2 → CH4 + 2H2O
Comparison of Figure 5-14 and Figure 5-15 leads to the following conclusions with respect to the redox
evolution of the Wallaby system.
1. Early CC_Bi_MT (calcite-biotite-magnetite) formed in oxidized conditions (SO2 or SO42-
dominant) with minor oxidation of CH4.
2. ACCH (calcite - chlorite) and reduced/acid (paragonite - muscovite - chloritoid) alteration
formed at highly reducing conditions with H2 the dominant reductant.
3. AMTA (magnetite - amphibole ± epidote ± calcite ± biotite) assemblages formed over a range
of redox conditions between these extremes.
4. Au lodes formed over a range of redox conditions with oxidized sulphur species (SO2 or SO42-
)
dominant over reactants (CH4, H2) in the haematite-associated lodes and reductants dominant
over oxidized sulphur species in the sinistral-slip lodes.
5. High grade Au (>10 ppm) formed in a very narrow range of conditions with CO2 >> CH4, H2
>> SO2 or SO42-
57
Comparison of the spectral and stable isotopic characteristics in WB0801CD (Figure 5-8 through Figure
5-10) shows that there are systematic changes in the isotopic characteristics that may be related to
silicate alteration mineralogy and indicate a progressive decrease in the redox state of the system with
depth in WB0801CD. There is a general trend of increasing δ34
S sulfide with depth with negative values
of δ34
S pyrite occurring within the O-NA and transitional assemblages (phlogopite/anhydrite ±
amphibole ± epidote ± magnetite; epidote ± magnetite ±phlogopite ± phengite ± chlorite) above ~ 700m
and δ34
S values for pyrite and pyrrhotite mostly between 0 and 5 ‰ in R-A assemblages below 700 m.
The most negative values of both δ34
S pyrite and δ13
C of carbonate (~ -5 to -7.5‰) overlap at 100 – 220
m depth in the uppermost gold zone in WB0801CD. Such correlations imply oxidation of CH4 to CO2 in
a highly oxidized environment. This interval also records positive values of δ34
S pyrite and δ13
C
carbonate with alteration assemblages dominated by amphibole ± chlorite ± magnetite which is
interpreted as a transitional assemblage between reduced and oxidized conditions, consistent with the
isotopic evidence for significant variation between reduced and oxidized conditions. A phlogopite -
anhydrite assemblage at ~ 40 to ~125m partly overlaps the transitional assemblage.
Positive values of δ34
S pyrite and δ13
C carbonate occur with the chloritoid ± paragonite ± muscovite
assemblages at ~1040 to 1230m, implying these assemblages formed in highly reducing conditions. The
acidic nature of the fluids implies that as well as H2 they contained high levels of acid volatiles, e.g.
HCl.
The progressive increase of δ13
C carbonate down hole is consistent with the sulphur isotopic evidence
for a progressive decrease in the redox state of the system with depth in WB0801CD and that the
chloritoid zone immediately beneath Thet’s Fault was a focus of reduced and acidic fluid flow.
Elevated δ18
O carbonate values (> 15‰) occur in both the transitional zone at 100 – 220 m depth and
the chloritoid zone (Figure 5-10). Elevated δ18
O carbonates values are interpreted to reflect a CO2±CH4
± H2 fluid with little water (Walshe and Neumayr, 2009) and imply a flux of anhydrous, volatile rich
fluids in both zones.
5.5 DISCUSSION AND CONCLUSIONS
Integration of the hyperspectral logging with stable isotope and structural constraints (Miller, 2005)
provides a framework to understand the 4D chemical evolution of the Wallaby system. This evolution is
summarized in Figure 5-16 and the salient changes in fluid redox and pH are summarized in Figure
5-17. Stage I was dominated by oxidized fluids with stage II proving evidence of transition between
oxidized and reduced fluids. Stage III was dominated by reduced fluids that were also acidic. This stage
58
Figure 5-16: Alteration and fluid evolution of the Wallaby deposit.
also shows the first hints of anhydrous- and volatile-rich fluids, as evidenced by elevated δ18
Ocarbonate
values (> ~15‰). The acidic alteration is interpreted to result from the dissolution of reduced,
anhydrous volatiles (H2, HCl) into local basinal waters within the major regional shears. This extensive
and intensive alteration had the effect of sealing many of these structures so that they subsequently
acted as aquitards rather than fluid conduits. Anomalous Au grades developed during this event. The
major Au stages (Stage IV & V) that followed the sealing of the architecture show evidence of both
reduced and oxidized fluids with the reduced fluids dominating in Stage V. High grade Au (>10gms) is
associated with elevated δ18
Ocarbonate indicating anhydrous, volatile-rich fluids were dominant over
hydrous fluids in the system at this stage (Walshe and Neumayr, 2009). Sustained coexisting hydrous
and anhydrous fluids (2 fluid phase conditions), through sustained high volatile pressures and limiting
influx of aqueous basinal fluids, appear to have been important pre-conditions for deposition of high
grade Au. The dominance of CO2 over other anhydrous volatiles at this stage supports these
conclusions. The presence of albite implies less acidic fluids (neutral to alkaline) perhaps reflecting the
lower water activity of this stage. Au deposition probably occurred through the breakdown of anhydrous
gold species in the hydrous environment under two-phase conditions. In the hydrous ± more acidic
conditions of earlier stages Au was mobilized through the system.
59
Figure 5-17: Redox/pH conditions of formation the Wallaby Deposit.
Stage 1: Early calcite-biotite-magnetite veins (“magmatic calcite veins”).
Stage II: AMTA: Magnetite-amphibole±epidote±calcite±biotite mantling syenite dykes.
Stage III: ACCH (calcite - chlorite) and reduced/acid (paragonite - muscovite - chloritoid) alteration.
Stage IV: Hm associated lodes: Quartz-carbonate-muscovite-albite-hematite.
Stage V: Sinistral-slip lodes: Quartz-carbonate-muscovite-albite-pyrite-fuchsite.
It is suggested that a better understanding of
the transitions from the proximal gold environments to distal reduced/acidic environments
the lateral zoning within the Wallaby deposit at stages IV and V
would enhance the understanding of the 4D chemical architecture of the Wallaby system and aid
targeting close to the Wallaby deposit and in other late-basin settings.
60
61
6 BULLANT AU MINE: A 3D MINERAL SYSTEM
PERSPECTIVE
6.1 INTRODUCTION
A hyperspectral study of five drill holes from the Bullant Au deposit (BUGD049, BUGD158,
BUGD162, BUGD166 and BUGD167) was undertaken as part of M373 (Huntington et al., 2007). Here
we re-examine these data in the light of a developing understanding of the Late Archean Au systems.
We focus on using the hyperspectral to define lithology, structure and key alteration assemblages that
help define the chemical gradients in the system and proximity to Au.
The Bullant Au deposit occurs within shear zones in mafic rocks that have been classified as basalts or
pillow basalts. The M373 study mapped the relative proportions and spatial distribution of the following
minerals: chlorite, carbonate, white mica, tourmaline, quartz, amphibole, biotite and epidote. The TIR-
Logger also detected quartz and albite, as well as epidote, at least two varieties of amphibole, chlorite,
carbonate and gypsum. The dominant mineralogy of the basalt is chlorite and amphibole with
superimposed quartz carbonate zones which appear variously mineralised.
6.2 LITHOLOGY
The boundaries between the basalt and pillowed basalt are inferred from the 2325nm wavelength
(Figure 6-1 and Figure 6-2) with the pillowed basalt defined by the shorter wavelengths (cooler
colours). For BUGD049 there is a good correlation between observed change from basalt to pillow
basalt and shift in the 2325nm wavelength as summarized below:
Observed break 2325nm down-hole wavelength shift
Basalt/pillow basalt ~ 96m ~85 to 98m to shorter
Pillow basalt /basalt ~ 130m ~ 129m to longer
Basalt/pillow basalt ~ 142m ~ 142m to shorter
Pillow basalt /basalt ~ 155m ~ 155m to longer
62
Figure 6-1: Leapfrog® model looking to the northwest.
A: Pfit of 2325nm wavelength (warm colours, 2340-2353 ; cool colours, 2318-2336) B: Lithology as logged.
grey: basalt, green: pillowed basalt, red: veins, magenta: intensely altered rocks.
Figure 6-2: Leapfrog® model looking to the northeast.
63
Figure 6-3: Leapfrog® model looking to the north A: Au grades B. Metasomatic amphibole.
Amphibole defined by an auxiliary match referenced to amphibole in sheared hosted amphibole in
BUGD049.
Figure 6-4: Leapfrog® model A: Prehnite B. Amphibole (squares) with prehnite (spheres).
The correlation is also good for BUGD162. Discrepancies in the correlation between the spectral
classification of lithology and company geological records for BUGD158 and BUGD167 were not
64
resolved. The upper and lower basalt/pillow basalt contacts, as defined in the 3D model, strike ~ 330°
and dip steeply.
6.3 MINERALIZED SHEARS
In BUGD049 good gold grades occur within an amphibole - biotite shear at ~ 177 - 182m and within an
amphibole -prehnite shear at ~ 194-198m (Figure 6-3A). Gold also occurs along the footwall contacts of
the pillow basalt in BUGD166 and BUGD049 and on the hangingwall contacts in BUGD167 and
BUGD049. The distribution of amphibole, assumed to be related to metasomatic processes (Figure
6-3B), was defined by an auxiliary match referenced to the amphibole-biotite-gold shear in BUGD049.
Linking the amphibole-biotite zone in BUGD049 to similar zones in BUGD158 BUGD162, BUGD166
and BUGD167 defined the orientation of amphibole-biotite shear as N-S striking and steeply east
dipping. The shear was analysed for Au in BUGD049 only. Figure 6-4A shows the distribution of
prehnite defined by the depth of 1478 nm feature. Prehnite occurs in the upper sections of the diamond
holes in the basalt or below the amphibole-biotite shear. Prehnite occurs with amphibole in the lower Au
zone in BUGD049 at ~ 194-198m. This zone has been linked to prehnite occurrences near the bottom of
BUGD158 and BUGD162 to create the prehnite shear. This shear was also analysed for Au in
BUGD049 only.
Figure 6-5: Leapfrog® model A: Epidote-clinozoisite B: Biotite C. Anhydrite-gypsum.
Epidote-clinozoisite defined from variation in 1550nm feature; epidote: cool colours – less than ~ 1550nm;
clinozoisite: warm colours – greater than ~1550nm. Distribution of biotite from TSA dark mica weights and
anhydrite-gypsum from TSA weights.
65
6.4 DISCUSSION OF ALTERATION MINERALS & CHEMICAL
GRADIENTS
The distribution of alteration assemblages may be used to determine the chemical gradients in mineral
systems. As discussed in section 4.3 the transition from alteration assemblages that include clinozoisite -
chlorite through to assemblages that include epidote ± phlogopite ± anhydrite marks a transition from
reduced to oxidized fluid conditions. Clinozoisite forms in a more acidic fluid environment compared
with epidote. On the basis of stoichiometry, prehnite could be anticipated to form in intermediate pH
conditions relative to clinozoisite and epidote. Amphibole forms in more reduced and alkaline
conditions relative to epidote ± biotite and more alkaline conditions relative to chlorite (Figure 5-17).
Figure 6-6: Chemical gradients in the Bullant Au system.
Despite the limited number of drill holes examined from the Bullant deposit it is possible to make some
assessment of the chemical gradients in the system based on the distribution of minerals determined
from the M373 Hylogger campaign. Most epidote - clinozoisite occurs in the upper basalt with more
limited occurrences below the amphibole shear (Figure 6-5A). In the upper basalt there is a tendency for
the proportion of epidote (cool colours) to clinozoisite (warm colours) to increase with depth. Biotite
66
also occurs in the upper basalt sections of the holes with epidote and anhydrite consistent with a more
oxidized and near-neutral to alkaline conditions in the basalt in vicinity of the upper contact with the
pillow basalts (Figure 6-6). Outboard of this, in the upper sections of the diamond holes, clinozoisite ±
prehnite is indicative of transition to more reduced and acidic conditions. Although not as well defined,
an approximately inverse spatial relationship exists below the amphibole shear as illustrated in Figure
6-6.
Amphibole distribution is generally antipathetic to the prehnite (Figure 6-4B) and focused in the central
sections of the diamond holes. The amphibole-biotite shear defines the lower limit of amphibole, with
the exception of the occurrence in the prehnite shear in BUGD049. The general inverse relationship of
amphibole to prehnite ± clinozoisite implies the zone focused on the pillow basalt was more alkaline
and reduced.
Biotite ± anhydrite occurs between the amphibole-phlogopite shear and the lower contact of the pillow
basalt where it overlaps with amphibole and gold zones. This spatial overlap of assemblages indicative
of reduced and oxidized conditions proximal to Au mineralization is consistent with Au precipitation
being controlled in part by redox gradients.
More extensive mapping of these gradients would aid future exploration.
67
7 NI LATERITE
7.1 INTRODUCTION
Spectra from a 2007 HyChips campaign were reviewed in order to assess spectral parameters that would
aid in Ni laterite exploration. Preliminary spectral investigation of the Jump Up Dam prospect revealed
that prospective rock-types may be extracted. Spectra from high-grade Ni Goongarrie samples were also
successfully matched with those in the Jump Up Dam dataset.
Further investigation turned to being able to add to the Material Type Classification Scheme that is
currently solely derived from whole-rock geochemistry. The objective of this research component was
to test the applicability of ASD spectra to independently classify mineralogical units at Jump Up Dam,
and therefore potentially be used as a low-cost alternative to whole-rock geochemistry.
Another objective was to statistically assess the spectral variability of individual samples. Within a
given sample, only a relatively small proportion of a sample is usually measured by hyperspectral means
even though mineralogy may vary greatly throughout a sample. Sampling protocol may help in
selecting a representative sample, but it is equally important to understand the potential variability in
mineralogy and what effect that has on the spectra.
The final objective was to compare and contrast coarse residue and pulp spectra measured from the
same sample.
7.2 METHODOLOGY
Hylogging of laboratory coarse residues from 235 Reverse Circulation (RC) drill samples consisting of
~30 samples of each of the 8 ore types based on the geochemical classification scheme of Heron
Resources. Sixty (8 samples x120) scans of each coarse residue and one spectrum per pulp were carried
out. Heron provided full XRF geochemistry and material type classification coding for the samples.
Heron retrieved the samples from storage, loaded samples into chip trays and transported them to Perth.
Principal components analysis was used to discriminate coherent mineralogical populations and end-
member assemblages amongst the ~14,500 coarse residue spectra. The same classification was applied
to the pulp spectra to determine whether the spectral classification was transferrable.
68
In order to assess spectral variability, numerical data were derived from several absorption features
contained within the VNIR-SWIR spectrum, with each numerical index common to all spectra that were
measured. Numerical indices selected were those commonly used in spectral interpretation, including
those that measured the depth and wavelength position of individual absorption features and depth ratios
of multiple absorption features.
The relative standard error (RSE) is the standard error of the mean (SEM) divided by the sample mean
expressed as a percentage, and was selected as the common measure of spectral variability. The SEM
was calculated by dividing the sample standard deviation by the square root of the sample size:
SEM = s ∕ √n
where
s is the sample standard deviation (sample-based estimate of the standard deviation of the
population), and
n is the size (number of spectra) of the sample.
The first exercise in assessing spectral variability was to plot the change in RSE with respect to sample
size, which aimed to predict the optimum rate of spectral sampling. For statistical and practical
purposes, the spectrum of RSE measurements needed for this assessment (between 3 and 120 samples)
was only calculated from the 8 samples that had an associated 120 spectral measurements. Secondly,
changes in RSE within a standard suite of spectral indices were compared against each spectral
classification. Samples that had significant numbers of empty chip tray compartments (2 samples) were
excluded from analysis. RSE from samples that lacked corresponding geochemistry/material type
classification (8 samples) were still compared to the spectral classifications.
7.3 RESULTS
The assessment of ten PC bands calculated from PC analysis of the entire VNIR-SWIR spectrum led to
the selection of four of these bands for subsequent spectro-mineralogical classification. Two scatter
plots were produced from which 14 unique spectral parameters were characterized using a combination
of the TSG mineral library (TSA) and independent algorithms. The PC_2 and PC_5 scatter plot aided in
the classification of 7 parameters; poorly crystalline kaolinite (Kaol PX – TSA) + Fe-Mg smectite
abundance >0.05, montmorillonite (TSA) + Al smectite abundance >0.06, diaspore (TSA) + ferric oxide
abundance <0.001, phlogopite (TSA), poorly ordered kaolinite (Kaol PX – TSA) + ferric oxide
abundance >0.16, Opaques_1 >0.8 and Kaolinite PX (TSA) + Opaques_1 >0.45 (Figure 7-1). PC_7 and
69
Figure 7-1: Scatter plots with Principal Component (covariance) bands 2 and 5.
Plots calculated from the full VNIR-SWIR reflectance spectrum – on each axis that shows each of the
spectro-mineralogical classifications. Plots are from left to right down the page; all spectra coloured by
Material Type, poorly-crystalline kaolinite (Kaol PX – TSA) + Fe-Mg smectite abundance >0.05,
montmorillonite (TSA) + Al smectite abundance >0.06, diaspore (TSA) + ferric oxide abundance <0.001,
phlogopite (TSA), poorly-ordered kaolinite (Kaol PX – TSA) + ferric oxide abundance >0.16, Opaques_1
>0.8 and Kaolinite PX (TSA) + Opaques_1 >0.45.
70
PC_9 bands helped characterize an additional 7 parameters; kaolinite abundance >0.12 + ferric oxide
abundance >0.12, kaolinite abundance >0.12 + ferric oxide abundance 0.089-0.12, kaolinite abundance
>0.12 + ferric oxide abundance 0.05-0.089, Magnesite+MagnesiumClays (TSA) + 1650 >0.43, Talc
(TSA) + kaolinite abundance >0.015, Talc (TSA) + ferrous iron abundance >0.1 and Hornblende (TSA)
+ 2350D >0.134 (Figure 7-2). Each of the spectral parameters characterized statistical “outliers” that
only amounted to a small proportion of the dataset in comparison to the bulk of the samples that were
predominantly made up of TSA(SWIR)-identified Serpentine (4210 spectra), Magnesium Clays (3982
spectra), Hornblende (1154 spectra), Kaolinite PX (901 spectra), Montmorillonite (724 spectra), Siderite
(427 spectra), Magnesite (382 spectra), MgChlorite (356 spectra), Kaolinite WX (347 spectra),
Palygorskite (326 spectra), Dolomite (292 spectra) and Talc (259 spectra).
There was generally poor transferability of the coarse residue spectral classifications to the pulp spectra
due to two factors. Firstly, many of the depth thresholds applied within the coarse residue dataset were
too high to be used to detect equivalent pulp samples; e.g. the Hornblende (TSA) + 2350D >0.134
needed to be reduced to >0.07. Secondly, where there were matches in the depth threshold, the TSA
mineral prediction between coarse residue and pulp spectra did not match. Typically, TSA mineral 1
and 2 were interchanged between spectra measured from different size fractions. A selection of
parameters was chosen to test what effect, if any, contrasting spectral extraction methods have on the
RSE. Parameters were chosen from the range of standardized products available from the Centre of
Excellence for 3D Mineral Mapping (C3DMM). These included a series of extracted depths of various
absorption features throughout the VNIR-SWIR spectrum, including Fe-Mg smectite abundance (2245-
2330 nm), 2350D, 1900D and 1650. Other parameters included a ratio of the depths of two features –
Opaques_1 (450 and 1650 nm) – and a measure of the variation in the minimum wavelength of the 1900
nm feature (1900wvl). All samples had exceptionally low RSE for 1900wvl and low RSE for
Opaques_1 compared to other parameters, except for sample H149457 where Opaques_1 had the
highest RSE of all parameters for all sampling rates (Figure 7-3). All depth extractions varied in their
relative RSE from sample to sample, with no one parameter consistently claiming the relatively highest
RSE values.
For each of the spectral classifications, the variation in RSE between indices trialled in Figure 7-3
generally correlated well with the range of expected values for a spectral sampling rate of 60. In the
main, RSE does not exceed ~3%, but “phlogopite” that wasn’t part of the dataset for comparisons
between RSE and sampling rate exhibited a broad range of RSE values for all indices, including 0.7-8.1
for 1900D.
71
Figure 7-2: Scatter plots with Principal Component (covariance) bands 7 and 9.
Plots calculated from the full VNIR-SWIR reflectance spectrum – on each axis that shows each of the
spectro-mineralogical classifications. Plots are from left to right down the page; all spectra coloured by
Material Type, kaolinite abundance >0.12 + ferric oxide abundance >0.12, kaolinite abundance >0.12 + ferric
oxide abundance 0.089-0.12, kaolinite abundance >0.12 + ferric oxide abundance 0.05-0.089,
Magnesite+MagnesiumClays (TSA) + 1650 >0.43, Talc (TSA) + kaolinite abundance >0.015, Talc (TSA) +
ferrous iron abundance >0.1 and Hornblende (TSA) + 2350D >0.134.
72
Figure 7-3: Line graphs showing variation in RSE with respect to sample size (rate).
Sample names are shown in each plot title, and were chosen as because they were the only samples that had
120 spectra collected for each. A mix of depth, wavelength and depth ratio indices (legend) were selected
from various parts of the spectrum to show coupled spectral-sampling variability between samples.
73
7.4 DISCUSSION
The spectro-mineralogical classification of the Jump Up Dam samples was based on silicate and
carbonate mineralogy, but the VNIR part of the spectrum has the capability to detect oxide minerals
also. The suggested methodology going forward would be to select mineralogical standards that were
highlighted from this study – in conjunction with additional oxide interpretation – and collect
accompanying petrography, XRD, microprobe, etc. combined with techniques including the Auxmatch
feature in TSG to further classify the mineralogy by hyperspectral means.
The difference in the intensity of absorption features between coarse residue and pulps stems from a
relationship between spectral reflectance and the grainsize of the sample. TSA classification has
limitations because the dominant versus subordinate mineral prediction may deviate substantially
between coarse residue and pulp because at the latter size fraction the softest mineral in the sample
preferentially coats harder minerals, leading to a non-representative sample. Due to the common use of
absorption feature depth in spectral classification, the effect of mineral bias with increasingly small size
fractions, combined with the attempt to transfer spectral classification from coarse residue to pulps,
suggests that classification should be redefined when changing grainsizes. Another factor that may lead
to a lack of success in transferring spectral processing is that even though each classification may be
based on between 60-180 spectra, the total number of samples is only 1-3. Given that the number of
samples to spectra is 1:1 in the case of the pulps, the likelihood of being able to successfully apply each
classification to such a low number of spectra is small.
The spectro-mineralogical classifications were mainly robust for coarse residue spectra in that there was
little to no variation in RSE for each across the range of tested spectral indices. The only exception was
the “phlogopite” classification that may suggest that the RSE method is a useful check on the validity of
grouping particular spectra into a single spectro-mineralogical classification. “Phlogopite” was also
classified in a large number of samples that may explain the broad range in RSE. Nevertheless, this
would suggest a substantial amount of intra-sample variation in spectral classification that may reflect
mineralogical heterogeneity or an unreliable classification method. The numerical ranges in Table 7.1
suggest that a similar test of RSE for a sampling rate of 3 spectra/sample would yield comparable results
to that found in Figure 7-3.
74
Table 7.1. Variation in RSE between spectral parameters; 1650, 1900D, 1900wvl, 2350D, Fe-MgSmectite and
Opaques_1 with respect to each of the spectro-mineralogical classifications. RSE is based on 60
spectra/sample.
Parameter % RSE
RSE_1650 RSE_1900D RSE_1900wvl RSE_2350D RSE_Fe-MgSmectite RSE_Opaques_1
PX Kaol + Fe-
MgSmectite >0.05 1.2 0.8 0.005 1.8 2.0 0.7
PX Kaol +
Opaques_1 >0.45 2.8 2.0 0.007 3.8 1.8 1.1
Diaspore + Fe oxide
abundance <0.001 0.9-1.2 0.5-0.8 0.002-0.004 0.4-0.6 0.8-0.9 0.2-0.4
Montmorillonite +
Al smectite
abundance >0.06
3.5 0.7 0.008 2.9 3.9 1.8
PX Kaol + Fe oxide
abundance >0.16 0.9-1.2 0.3-0.7 0.003-0.005 2.6-4.4 2.6-3.3 1.2-1.4
Opaques_1 >0.8 0.9-1.4 0.2-1.7 0.004-0.02 0.9-3.4 0.9-2.0 0.2-0.9
Phlogopite 0.9-6.7 0.7-8.1 0.006-0.03 0.5-5.6 1.1-8.4 0.4-2.5
Kaol abund. >0.12+
Fe oxide abund.
>0.12
0.9 0.3 0.006 0.7 0.8 0.6
Kaol abund. >0.12+
Fe oxide abund.
>0.089-0.12
0.8 0.6 0.009 1.3 1.3 1.1
Kaol abund. >0.12+
Fe oxide abund.
>0.05-0.089
0.8-1.0 0.6-1.0 0.009-0.01 0.8-1.3 0.8-1.5 1.1-1.4
Magnesite +
magnesium clays +
1650 >0.43
0.8-1.2 2.0-2.7 0.01-0.04 2.3-3.4 1.2-2.0 0.3-2.1
Talc + Fe oxide
abund. >0.1 0.6 0.9 0.002 0.4 0.4 0.6
Talc + Kaol abund.
>0.016 1.1 3.6 0.02 1.2 1.2 1.4
Hornblende +
2350D >0.134 1.1-1.4 0.5-1.6 0.002 1.0-1.6 1.0 0.5-0.6
75
8 PHOSPHATE
VNIR-SWIR and TIR spectroscopy methods were trialled as a means to detect apatite and other
phosphorus-bearing minerals. Initial tests upon mineral library apatite specimens revealed that each
apatite had different VNIR-SWIR vibrational responses due to varying degrees of F, Cl and OH
substitution. A follow-up program that measured VNIR-SWIR spectra of phosphorite samples from the
Phosphate Hill/Duchess Deposit in Western Queensland failed to find a spectral correlative to phosphate
wt%. However, TIR measurements of the mineral library apatites found that spectra from most of the
samples matched pure apatite spectra from the Arizona State University. The diagnostic apatite
absorption doublet with peaks at 9.2 and 9.4 µm was present within samples containing quartz and
carbonate, which is a typical phosphorite assemblage. The potential for infrared spectra to be applied to
phosphorite exploration lies in the future quantification of apatite abundance from TIR spectra,
especially within mixed mineral rocks. The introduction of automated TIR loggers for commercial use
will enable relatively low-cost and rapid detection of anomalous phosphorite mineralization.
8.1 INTRODUCTION
Phosphorite exploration, like many other mineral exploration endeavours, is always seeking low-cost
alternatives to traditional exploration practises in order to drive down discovery costs. Reflectance
spectroscopy is an ever-expanding technology that provides a cheap as well as a rapid solution for the
detection of mineralization. The aim of this section is to examine the suitability of Visible to Near
InfraRed (VNIR), Short-Wave InfraRed (SWIR) and Thermal InfraRed (TIR) spectroscopy applied to
phosphorite exploration.
8.2 METHODS
8.2.1 Research rationale and background
A previous PIMA study showed that the major absorption features within phosphate SWIR spectra are
at ~2150nm, 2220nm, 2314nm and 2344nm, although each of the spectra varied in features present
(Integrated Spectronics 1993) , and hinted that this change could be a result of F, Cl and OH
substitution. The REE response of apatite can be seen as numerous sharp features in the Visible to Near
Infrared (VNIR) between 500-900nm (0.5-0.9 micron), and is potentially the most diagnostic indicator
of apatite in the VNIR-SWIR.
76
8.2.2 Sampling
VNIR-SWIR spectra (350-2500 nm) and TIR spectra (7000-14000 nm) were collected from ten apatite-
bearing samples within the Mitchell Collection housed at the Australian Resources Research Centre
(ARRC). VNIR-SWIR spectra were collected on a FieldSpec 1 from Analytical Spectral Devices
(ASD) Inc., and TIR spectra were taken from a micro Fourier Transform InfraRed (FTIR) spectrometer.
Pure apatite spectra from the Jet Propulsion Laboratory (JPL) at the California Institute of Technology
and Arizona State University (ASU) were used as standards in the interpretation of ASD and microFTIR
spectra, respectively.
The second part of the project comprised VNIR-SWIR spectra measurement of samples collected from
the Duchess/Phosphate Hill deposit, NW Queensland. The samples are part of a PhD thesis collection at
James Cook University (Hough, 2004). The same Fieldspec 1 instrument as was used in the initial
measurement was used to collect spectra from 89 samples; 85 of which had corresponding whole-rock
XRF.
8.3 RESULTS
FTIR measurement of the Mitchell Collection apatites revealed spectra with a diagnostic absorption
“doublet” at ~9000 and ~9500 nm (Appendix 4). Samples also contained absorption features diagnostic
of quartz and calcite. Two samples – M0972 and M1158 – did not contain recognizable apatite
absorption features, but other absorption features (calcite for M0972) suggest that these samples need
re-classification through other means, e.g. XRD, petrography. ASD spectra - similarly to past PIMA
studies - are quite variable and diagnostic absorption features are relatively difficult to assign.
ASD spectra from the collection of Hough (2004) were analyzed via Principal Components Analysis
(PCA) within TSGTM
. Spectra were sub-divided into VNIR and SWIR bands and PCA calculated on
each. End members derived from PCA show little to no correlation with P2O5 from whole-rock XRF
(Figure 8-1). Within the VNIR, three main classes of spectra were identified from the end member
classification (Figure 8-2). Previous investigation into the applicability of SWIR spectra applied to
phosphorites found a strong negative correlation between the ratio of the depth of features at 2212 and
1932 nm (d2212:d1932), and P2O5 abundance (Wells & Ramanaidou 2001). In contrast to this finding,
the same SWIR parameter applied to the Hough (2004) collection found only 73 out of a total 293
spectra contained absorption features at 1932 nm and 2212 nm, and of these 73 spectra there was no
correlation between d2212:d1932 and P2O5 (Figure 8-3).
77
Figure 8-1: End-member classification from PCA Vs whole-rock % P2O5 plots.
Points coloured by lithology. a) VNIR (500-900 nm). b) SWIR (2100-2500 nm).
Figure 8-2: Spectra representative of VNIR end-member classification.
a) Class 4. b) Class 9. c) Class 10.
78
Figure 8-3: Ratio of depths of 2212 and 1932 nm features (d2212/1932) vs % P2O5.
Points coloured by lithology
8.4 DISCUSSION
The inconsistency in ASD spectral signature of apatite-bearing samples is probably due to the highly
variable composition of apatite, and the associated substitution of Cl-F-OH that would cause differences
in the vibrational response. In addition to this various components can substitute for PO4 including S,
CO2, and As, then the Ca site can contain REE, Na, Ba, U etc. The contrast in d2212/d1932 Vs % P2O5
between this and previous studies can only be explained due to higher sample complexity and a possibly
more lithologically diverse sample set in the latest study compared to the earlier example, because both
sample suites were derived from the Duchess deposit.
% P2O5
79
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Appendix 1: Microprobe Data
A-1
APPENDIX 1Amphiboles
Sample Number SiO2 TiO2 Al2O3 Cr2O3 FeO MnO MgO CaO Na2O K2O F Cl O=F O=Cl Total Si Ti Al Cr Fe3+ Fe2+ Mn2+ Mg Ca Na K F Cl Tot. Cat.Genetic
Classification Sample Drill hole depth w2330 D23902300-2400 pfit d/FeOH pfit d
M400_010Amph2p1 52.74 0.071 4.18 0 8.96 0.248 16.84 12.22 1.17 0.087 0 0 0 0 98.604 7.574 0.008 0.707 0 0.028 1.048 0.03 3.605 1.88 0.326 0.016 0 0 15.222 Metamorphic T.S. block UDD1420 83.973 2322.89 0.0681 3.825581395M400_010Amph2p2 52.77 0.235 4.21 0.022 9.36 0.229 16.83 11.96 1.264 0.085 0.016 0.019 0.007 0.004 99.075 7.536 0.025 0.709 0.002 0.143 0.975 0.028 3.583 1.83 0.35 0.015 0.007 0.005 15.195 Metamorphic T.S. block UDD1420 83.973 2322.89 0.0681 3.825581395M400_010Amph2p3 53.38 0.109 3.69 0.02 7.79 0.283 17.46 12.19 1.08 0.094 0.003 0 0.001 0 98.202 7.659 0.012 0.624 0.002 0 0.935 0.034 3.734 1.874 0.3 0.017 0.001 0 15.191 Metamorphic T.S. block UDD1420 83.973 2322.89 0.0681 3.825581395M400_010Amphp1 53.54 0.108 2.69 0.023 11.07 0.182 16.26 11.49 0.965 0.035 0 0 0 0 98.449 7.694 0.012 0.456 0.003 0.316 1.014 0.022 3.483 1.769 0.269 0.006 0 0 15.045 Metamorphic T.S. block UDD1420 83.973 2322.89 0.0681 3.825581395M400_010Amphp2 51.2 0.22 5.08 0.048 10.29 0.244 15.46 11.81 1.51 0.079 0 0.01 0 0.002 98.035 7.458 0.024 0.872 0.006 0.031 1.222 0.03 3.357 1.843 0.426 0.015 0 0.002 15.284 Metamorphic T.S. block UDD1420 83.973 2322.89 0.0681 3.825581395M400_010Amphp3 53.59 0.126 2.67 0.007 10.67 0.125 16.21 11.61 1.066 0.045 0.059 0 0.025 0 98.268 7.738 0.014 0.454 0.001 0.142 1.146 0.015 3.489 1.796 0.298 0.008 0.027 0 15.103 Metamorphic T.S. block UDD1420 83.973 2322.89 0.0681 3.825581395
M400_011_amph1_pt1 45.37 0.175 12.05 0.091 12.47 0.23 12.79 11.88 2.15 0.119 0 0.003 0 0.001 97.327 6.496 0.019 2.033 0.01 1.048 0.445 0.028 2.73 1.822 0.597 0.022 0 0.001 15.249 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph1_pt2 51.38 0.035 5.81 0.057 10.06 0.198 16.2 12.42 0.943 0.053 0 0 0 0 99.267 7.298 0.004 0.973 0.006 0.505 0.69 0.024 3.431 1.89 0.26 0.01 0 0 15.09 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph1_pt3 50.12 0.074 7.33 0.077 10.55 0.18 15.34 12.44 1.242 0.062 0.006 0 0.003 0 99.531 7.122 0.008 1.228 0.009 0.58 0.674 0.022 3.25 1.894 0.342 0.011 0.003 0 15.139 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph2_pt1 44.38 0.132 13.02 0.082 12.55 0.272 12.41 11.64 2.44 0.146 0.037 0 0.016 0 99.211 6.368 0.014 2.202 0.009 1.168 0.338 0.033 2.654 1.789 0.679 0.027 0.017 0 15.282 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph2_pt2 43.62 0.151 14.07 0.128 12.99 0.25 11.65 11.44 2.54 0.205 0 0.021 0 0.005 99.16 6.276 0.016 2.386 0.015 1.172 0.39 0.03 2.499 1.763 0.709 0.038 0 0.005 15.294 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph2_pt3 45.35 0.093 12.28 0.096 12.45 0.219 13.16 11.45 2.33 0.151 0 0.003 0 0.001 99.693 6.448 0.01 2.058 0.011 1.21 0.27 0.026 2.79 1.744 0.642 0.027 0 0.001 15.237 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph3_pt1 45.81 0.143 12.02 0.186 12.38 0.283 12.91 11.36 2.36 0.151 0 0.003 0 0.001 99.723 6.522 0.015 2.017 0.021 1.093 0.381 0.034 2.74 1.733 0.651 0.027 0 0.001 15.236 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph3_pt2 46.68 0.089 10.41 0.174 11.79 0.24 14.1 11.4 2.17 0.06 0 0 0 0 99.22 6.645 0.01 1.747 0.02 1.147 0.256 0.029 2.992 1.739 0.599 0.011 0 0 15.194 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph3_pt3 46.76 0.124 10.36 0.191 11.5 0.217 14.36 11.33 2.27 0.049 0.017 0 0.007 0 99.276 6.64 0.013 1.734 0.021 1.176 0.189 0.026 3.04 1.724 0.625 0.009 0.007 0 15.198 Al-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph4_pt1 51.09 0.086 6.27 0.014 10.39 0.167 15.96 12.44 0.993 0.074 0 0 0 0 99.598 7.242 0.009 1.048 0.002 0.533 0.699 0.02 3.373 1.889 0.273 0.013 0 0 15.101 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph4_pt2 50.4 0.035 7.35 0.102 10.35 0.179 15.46 12.25 1.31 0.116 0 0.01 0 0.002 99.675 7.142 0.004 1.228 0.011 0.571 0.655 0.021 3.266 1.86 0.36 0.021 0 0.002 15.14 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph4_pt3 51.81 0.09 5.17 0.11 9.8 0.164 16.65 12.7 0.767 0.063 0 0.013 0 0.003 99.449 7.347 0.01 0.864 0.012 0.458 0.704 0.02 3.52 1.93 0.211 0.011 0 0.003 15.087 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph5_pt1 55.94 0 1.02 0 9.66 0.183 18.1 13.14 0.099 0 0.039 0.003 0.016 0.001 100.281 7.876 0 0.169 0 0.078 1.06 0.022 3.799 1.982 0.027 0 0.017 0.001 15.013 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph5_pt2 54.89 0 1.9 0 10.61 0.215 17.3 12.87 0.2 0.012 0 0.004 0 0.001 100.099 7.771 0 0.317 0 0.14 1.117 0.026 3.651 1.952 0.055 0.002 0 0.001 15.03 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_011_amph5_pt3 56.18 0.031 0.572 0.041 8.58 0.151 18.67 12.99 0.082 0.004 0 0.001 0 0 99.419 7.938 0.003 0.095 0.005 0.052 0.962 0.018 3.932 1.966 0.022 0.001 0 0 14.995 Si-amphibole T.S. block UDD1420 242.302 2313.5 0.0514 0.968319559M400_013_amph1_pt1 51.81 0.015 4.39 0.299 13.99 0.167 14.36 11.94 0.9 0.086 0 0.039 0 0.009 97.987 7.444 0.002 0.743 0.034 0.389 1.292 0.02 3.076 1.838 0.251 0.016 0 0.009 15.105 Metamorphic T.S. block UDD1420 266.946 2317.22 0.0195M400_013_amph1_pt2 52.24 0.094 4.18 0.216 14.32 0.151 14.47 11.9 0.823 0.057 0.006 0.041 0.003 0.009 100.594 7.456 0.01 0.703 0.024 0.462 1.247 0.018 3.079 1.82 0.228 0.01 0.003 0.01 15.058 Metamorphic T.S. block UDD1420 266.946 2317.22 0.0195M400_013_amph1_pt3 52.34 0.019 4.43 0.264 13.94 0.159 14.46 12.01 0.894 0.081 0 0.027 0 0.006 100.721 7.466 0.002 0.745 0.03 0.356 1.307 0.019 3.075 1.836 0.247 0.015 0 0.007 15.097 Metamorphic T.S. block UDD1420 266.946 2317.22 0.0195M400_013_amph2_pt1 41.12 0.082 14.77 0.938 15.36 0.193 9.24 11.87 2.46 0.509 0 0.036 0 0.008 98.68 6.081 0.009 2.574 0.11 1.106 0.793 0.024 2.037 1.881 0.705 0.096 0 0.009 15.416 Al-amphibole T.S. block UDD1420 266.946 2317.22 0.0195M400_013_amph2_pt2 41.6 0 14.4 1.072 15.59 0.184 9.13 11.87 2.37 0.471 0 0.023 0 0.005 98.813 6.149 0 2.509 0.125 1.047 0.88 0.023 2.012 1.88 0.679 0.089 0 0.006 15.394 Al-amphibole T.S. block UDD1420 266.946 2317.22 0.0195M400_013_amph2_pt3 41.61 0.067 14.83 0.764 16.12 0.195 9.38 11.84 2.48 0.478 0.075 0.025 0.032 0.006 99.939 6.071 0.007 2.55 0.088 1.214 0.754 0.024 2.04 1.851 0.702 0.089 0.035 0.006 15.39 Al-amphibole T.S. block UDD1420 266.946 2317.22 0.0195M400_014_amph1_pt1 54.98 0.067 1.514 0 12.8 0.225 16.71 12.02 0.376 0.022 0.038 0.014 0.016 0.003 100.858 7.817 0.007 0.254 0 0 1.522 0.027 3.542 1.831 0.104 0.004 0.017 0.003 15.108 Metamorphic T.S. block UDD1420 267.049 2319.08 0.0144 1.285302594M400_014_amph1_pt2 54.82 0.004 1.729 0.015 12.78 0.281 16.59 11.78 0.432 0.013 0 0.009 0 0.002 100.546 7.82 0 0.291 0.002 0 1.525 0.034 3.528 1.8 0.119 0.002 0 0.002 15.122 Metamorphic T.S. block UDD1420 267.049 2319.08 0.0144 1.285302594M400_014_amph1_pt3 55.58 0.041 1.231 0.007 12.01 0.231 17.04 12.47 0.258 0.018 0 0.015 0 0.003 101.011 7.86 0.004 0.205 0.001 0 1.42 0.028 3.592 1.889 0.071 0.003 0 0.004 15.074 Metamorphic T.S. block UDD1420 267.049 2319.08 0.0144 1.285302594M400_014_amph2_pt1 53.62 0.056 3.7 0.011 10.19 0.189 17.45 12.51 0.778 0.054 0 0.003 0 0.001 100.678 7.495 0.006 0.61 0.001 0.499 0.693 0.022 3.636 1.873 0.211 0.01 0 0.001 15.055 Si-amphibole T.S. block UDD1420 267.049 2319.08 0.0144 1.285302594M400_014_amph2_pt2 55.13 0.052 2.07 0.029 9.54 0.159 18.41 12.75 0.423 0.046 0.002 0.002 0.001 0 100.73 7.71 0.006 0.341 0.003 0.216 0.899 0.019 3.838 1.91 0.115 0.008 0.001 0 15.066 Si-amphibole T.S. block UDD1420 267.049 2319.08 0.0144 1.285302594M400_014_amph2_pt3 54.09 0.019 3.1 0.007 9.76 0.167 17.99 12.42 0.641 0.055 0.012 0 0.005 0 100.372 7.596 0.002 0.513 0.001 0.279 0.867 0.02 3.766 1.869 0.174 0.01 0.005 0 15.098 Si-amphibole T.S. block UDD1420 267.049 2319.08 0.0144 1.285302594M400_015_amph1_pt1 57.27 0.053 0.875 0.023 3.01 0.148 22.92 12.96 0.371 0.042 0.004 0.007 0.002 0.002 99.793 7.851 0.005 0.141 0.003 0.135 0.21 0.017 4.684 1.904 0.099 0.007 0.002 0.002 15.057 Si-amphibole T.S. block UDD1420 268.002 2305.76 0.018M400_015_amph1_pt2 57.07 0.049 0.749 0.005 2.84 0.157 22.59 13.16 0.377 0.06 0 0.008 0 0.002 99.178 7.865 0.005 0.122 0.001 0.18 0.148 0.018 4.641 1.943 0.101 0.011 0 0.002 15.034 Si-amphibole T.S. block UDD1420 268.002 2305.76 0.018M400_015_amph1_pt3 57.27 0.015 0.754 0.019 2.98 0.183 22.64 13.15 0.376 0.042 0 0.006 0 0.001 99.551 7.862 0.002 0.122 0.002 0.205 0.137 0.021 4.633 1.934 0.1 0.007 0 0.001 15.026 Si-amphibole T.S. block UDD1420 268.002 2305.76 0.018M400_015_amph2_pt1 57.62 0 0.074 0.012 6.2 0.206 20.7 13.27 0.058 0.014 0 0.026 0 0.006 100.29 7.987 0 0.012 0.001 0.009 0.709 0.024 4.278 1.971 0.016 0.002 0 0.006 15.01 Si-amphibole T.S. block UDD1420 268.002 2305.76 0.018M400_015_amph2_pt2 57.68 0.015 0.044 0.006 5.64 0.173 21.37 13.04 0.047 0.006 0.06 0.006 0.025 0.001 100.171 7.975 0.002 0.007 0.001 0.037 0.615 0.02 4.405 1.932 0.013 0.001 0.026 0.001 15.007 Si-amphibole T.S. block UDD1420 268.002 2305.76 0.018M400_015_amph2_pt3 57.3 0 0.06 0.016 6.18 0.231 21.04 13.17 0.029 0 0 0.008 0 0.002 100.119 7.94 0 0.01 0.002 0.109 0.607 0.027 4.346 1.955 0.008 0 0 0.002 15.004 Si-amphibole T.S. block UDD1420 268.002 2305.76 0.018M400_017_amph1_pt1 56.98 0.034 0.588 0 1.027 0.071 22.17 12.68 0.394 0.025 0 0 0 0 96.086 8.071 0.004 0.098 0 0 0.122 0.009 4.682 1.924 0.108 0.005 0 0 15.022 Si-amphibole T.S. block UDD1420 314.132 2313.73 0.0125M400_017_amph1_pt2 56.75 0.042 0.41 0.046 1.053 0.174 21.82 12.6 0.341 0.017 0 0 0 0 95.35 8.113 0.005 0.069 0.005 0 0.126 0.021 4.65 1.93 0.094 0.003 0 0 15.016 Si-amphibole T.S. block UDD1420 314.132 2313.73 0.0125M400_017_amph1_pt3 56.87 0.017 0.502 0.018 1.13 0.156 22.01 12.47 0.372 0.014 0 0 0 0 95.666 8.09 0.002 0.084 0.002 0 0.134 0.019 4.668 1.901 0.103 0.002 0 0 15.004 Si-amphibole T.S. block UDD1420 314.132 2313.73 0.0125M400_020_amph1_pt1 40.28 0.048 17.49 0 20.96 0.336 4.82 11.34 1.38 0.659 0 0.097 0 0.022 99.462 6.045 0.005 3.094 0 0.837 1.794 0.043 1.078 1.824 0.402 0.126 0 0.025 15.248 Al-amphibole T.S. block UDD1420 440.714 2330.54 0.0176M400_020_amph1_pt2 40.12 0.104 17.45 0.015 20.39 0.306 4.98 11.39 1.51 0.682 0.076 0.083 0.032 0.019 99.146 6.039 0.012 3.096 0.002 0.809 1.758 0.039 1.118 1.837 0.441 0.131 0.036 0.021 15.281 Al-amphibole T.S. block UDD1420 440.714 2330.54 0.0176M400_020_amph1_pt3 40.86 0.096 16.64 0.029 19.83 0.352 5.57 11.42 1.42 0.519 0.053 0.022 0.022 0.005 98.841 6.139 0.011 2.947 0.003 0.792 1.7 0.045 1.248 1.838 0.414 0.099 0.025 0.006 15.236 Al-amphibole T.S. block UDD1420 440.714 2330.54 0.0176M400_021_amph1_pt1 44.75 0.106 12.11 0.651 15.98 0.23 10.35 11.97 1.42 0.158 0.022 0.019 0.009 0.004 99.866 6.566 0.012 2.094 0.076 0.479 1.482 0.029 2.264 1.882 0.404 0.03 0.01 0.005 15.315 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph1_pt2 45.83 0.053 10.9 0.59 15.84 0.194 10.96 12.05 1.278 0.147 0.063 0 0.027 0 99.981 6.699 0.006 1.878 0.068 0.479 1.457 0.024 2.388 1.887 0.362 0.027 0.029 0 15.277 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph1_pt3 43.69 0.073 12.79 1.172 16.4 0.167 9.8 11.97 1.51 0.154 0.048 0 0.02 0 99.84 6.439 0.008 2.221 0.137 0.508 1.513 0.021 2.153 1.89 0.431 0.029 0.022 0 15.35 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph2_pt1 51.86 0.233 4.94 0.077 12.64 0.185 14.8 12.53 0.467 0.029 0.035 0 0.015 0 99.875 7.432 0.025 0.834 0.009 0.259 1.256 0.022 3.162 1.924 0.13 0.005 0.016 0 15.059 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph2_pt2 52.37 0.173 4.4 0.089 12.25 0.194 15.1 12.6 0.451 0.028 0.041 0 0.017 0 99.779 7.508 0.019 0.743 0.01 0.192 1.277 0.024 3.227 1.935 0.125 0.005 0.019 0 15.066 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph2_pt3 51.83 0.102 4.74 0.118 12.82 0.179 14.72 12.35 0.495 0.039 0.02 0.007 0.009 0.002 99.508 7.453 0.011 0.803 0.013 0.304 1.237 0.022 3.156 1.903 0.138 0.007 0.009 0.002 15.048 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph3_pt1 45.54 0.358 11.54 0.35 15.72 0.189 10.82 12.11 1.295 0.096 0.018 0.009 0.008 0.002 100.142 6.643 0.039 1.984 0.04 0.442 1.475 0.023 2.353 1.893 0.366 0.018 0.008 0.002 15.277 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph3_pt2 44.85 0.481 11.78 0.609 15.49 0.17 10.01 11.93 1.34 0.069 0.068 0.003 0.029 0.001 98.877 6.656 0.054 2.06 0.072 0.256 1.666 0.021 2.215 1.897 0.386 0.013 0.032 0.001 15.296 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_021_amph3_pt3 47.18 0.489 9.65 0.332 15.13 0.178 11.5 12.18 1.022 0.054 0 0 0 0 99.771 6.881 0.054 1.659 0.038 0.327 1.518 0.022 2.5 1.903 0.289 0.01 0 0 15.202 Metamorphic T.S. block UDD1420 459.766 2315.02 0.142 2.680798005M400_022_amph1_pt1 50.27 0.028 5.56 0.075 17.45 0.314 11.55 12.11 0.498 0.189 0.059 0.004 0.025 0.001 100.138 7.396 0.003 0.964 0.009 0.052 2.095 0.039 2.533 1.909 0.142 0.036 0.027 0.001 15.178 Metamorphic T.S. block UDD1420 475.549 2328.81 0.0427 2.450331126M400_022_amph1_pt2 47.22 0.02 8.23 0.129 19.91 0.449 9.57 11.96 0.789 0.261 0.051 0.006 0.022 0.001 100.659 7.003 0.002 1.438 0.015 0.261 2.209 0.056 2.116 1.9 0.227 0.049 0.024 0.001 15.276 Metamorphic T.S. block UDD1420 475.549 2328.81 0.0427 2.450331126M400_022_amph1_pt3 47.29 0.045 9.62 0.273 16.72 0.345 10.55 12.16 1.029 0.309 0.072 0.019 0.03 0.004 100.488 6.917 0.005 1.658 0.032 0.306 1.74 0.043 2.3 1.906 0.292 0.058 0.033 0.005 15.255 Metamorphic T.S. block UDD1420 475.549 2328.81 0.0427 2.450331126M400_024_amph1_pt1 54.29 0 2.79 0.021 9.74 0.205 18.06 12 0.485 0.03 0.045 0.001 0.019 0 99.725 7.705 0 0.467 0.002 0 1.156 0.025 3.821 1.825 0.133 0.005 0.02 0 15.139 Metamorphic T.S. block UDD1420 497.6 2311.05 0.118 5.130718954M400_024_amph1_pt2 54.28 0.004 2.9 0 9.2 0.23 17.92 12.04 0.554 0.014 0.014 0 0.006 0 99.246 7.645 0 0.481 0 0.441 0.643 0.027 3.762 1.817 0.151 0.003 0.006 0 14.971 Metamorphic T.S. block UDD1420 497.6 2311.05 0.118 5.130718954M400_024_amph1_pt3 53.64 0.033 3.19 0.001 9.65 0.208 17.65 12.19 0.583 0.016 0.052 0 0.022 0 99.302 7.66 0.004 0.537 0 0 1.152 0.025 3.757 1.865 0.161 0.003 0.023 0 15.164 Metamorphic T.S. block UDD1420 497.6 2311.05 0.118 5.130718954M400_025_amph1_pt1 50.81 0.02 4.03 0 19 0.269 11.28 11.88 0.601 0.135 0 0.024 0 0.005 100.138 7.528 0.002 0.704 0 0.037 2.318 0.034 2.492 1.886 0.173 0.026 0 0.006 15.198 Metamorphic T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph1_pt2 51.35 0.008 3.69 0.033 18.54 0.31 11.56 11.76 0.506 0.108 0 0.012 0 0.003 99.985 7.601 0.001 0.644 0.004 0 2.295 0.039 2.551 1.865 0.145 0.02 0 0.003 15.166 Metamorphic T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph1_pt3 52.38 0 2.71 0 18.53 0.261 12.28 11.96 0.364 0.043 0.07 0.011 0.029 0.002 100.69 7.672 0 0.468 0 0.077 2.193 0.032 2.681 1.877 0.103 0.008 0.032 0.003 15.111 Metamorphic T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph2_pt1 41.44 0 14.48 0.032 21.47 0.193 5.78 11.34 1.71 0.58 0 0.101 0 0.023 99.189 6.244 0 2.572 0.004 0.966 1.74 0.025 1.298 1.831 0.5 0.112 0 0.026 15.291 Al-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph2_pt2 41.27 0.065 15.38 0.008 22.07 0.26 5.48 11.35 1.64 0.544 0 0.093 0 0.021 100.228 6.154 0.007 2.703 0.001 1.034 1.718 0.033 1.218 1.813 0.474 0.103 0 0.023 15.259 Al-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485
A-2
M400_025_amph2_pt3 41.73 0.109 14.32 0 22.16 0.25 5.87 11.34 1.62 0.585 0 0.161 0 0.036 100.201 6.232 0.012 2.52 0 1.043 1.724 0.032 1.307 1.814 0.469 0.111 0 0.041 15.265 Al-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph3_pt1 42.31 0.055 15.29 0.005 22.23 0.262 5.69 11.52 1.69 0.323 0 0.053 0 0.012 101.492 6.209 0.006 2.645 0.001 1.029 1.699 0.033 1.245 1.811 0.481 0.06 0 0.013 15.218 Al-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph3_pt2 42.44 0.033 15 0.032 21.84 0.248 5.83 11.49 1.63 0.341 0 0.049 0 0.011 101.025 6.255 0.004 2.605 0.004 0.973 1.719 0.031 1.281 1.814 0.466 0.064 0 0.012 15.216 Al-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph3_pt3 42.16 0 15.21 0.001 22.16 0.255 5.72 11.38 1.64 0.353 0 0.055 0 0.012 101.027 6.215 0 2.642 0 1.043 1.689 0.032 1.257 1.797 0.469 0.066 0 0.014 15.21 Al-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph4_pt1 52.56 0 0.476 0.025 25.2 0.412 8.38 11.88 0.305 0.024 0 0.009 0 0.002 101.376 7.878 0 0.084 0.003 0.153 3.006 0.052 1.872 1.908 0.089 0.005 0 0.002 15.049 Si-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph4_pt2 51 0.015 0.99 0.03 25.55 0.386 8.72 11.54 0.142 0.044 0 0.005 0 0.001 100.536 7.696 0.002 0.176 0.004 0.416 2.809 0.049 1.962 1.866 0.042 0.009 0 0.001 15.029 Si-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph4_pt3 52.61 0 0.518 0.041 25.9 0.458 7.51 11.88 0.158 0.033 0 0.019 0 0.004 101.238 7.941 0 0.092 0.005 0.015 3.255 0.059 1.69 1.921 0.046 0.006 0 0.005 15.03 Si-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_025_amph4_pt4 52.67 0 0.523 0.057 24.04 0.393 8.4 11.85 0.17 0.025 0.047 0.007 0.02 0.002 100.272 7.945 0 0.093 0.007 0.093 2.94 0.05 1.889 1.915 0.05 0.005 0.022 0.002 14.986 Si-amphibole T.S. block UDD1510 59.1538 2329.31 0.0292 6.503067485M400_026_amph1_pt1 42.25 0.073 15.46 0.007 16.54 0.21 9.21 11.66 2.11 0.236 0.062 0.147 0.026 0.033 100.01 6.133 0.008 2.645 0.001 1.18 0.828 0.026 1.993 1.813 0.594 0.044 0.029 0.036 15.265 Al-amphibole T.S. block UDD1510 143.287 2318.74 0.118 6.788732394M400_026_amph1_pt2 42.56 0.093 15.22 0.036 16.53 0.191 9.26 11.62 2.27 0.192 0 0.128 0 0.029 100.12 6.163 0.01 2.598 0.004 1.175 0.826 0.023 1.999 1.803 0.637 0.035 0 0.031 15.275 Al-amphibole T.S. block UDD1510 143.287 2318.74 0.118 6.788732394M400_026_amph1_pt3 42.36 0.077 15.2 0.02 16.25 0.207 9.21 11.61 2.33 0.189 0 0.119 0 0.027 99.629 6.166 0.008 2.608 0.002 1.154 0.824 0.025 1.999 1.811 0.658 0.035 0 0.029 15.29 Al-amphibole T.S. block UDD1510 143.287 2318.74 0.118 6.788732394M400_027_amph1_pt1 54.16 0.088 2.62 0.021 10.52 0.355 16.71 12.55 0.257 0.122 0 0.014 0 0.003 99.495 7.708 0.009 0.439 0.002 0.202 1.05 0.043 3.545 1.914 0.071 0.022 0 0.003 15.007 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph1_pt2 54.78 0.084 1.804 0.068 10.42 0.411 17.36 13 0.185 0.07 0.061 0 0.026 0 100.331 7.76 0.009 0.301 0.008 0.091 1.144 0.049 3.666 1.973 0.051 0.013 0.027 0 15.063 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph1_pt3 54.24 0.061 2.34 0.079 10.55 0.45 16.98 12.72 0.214 0.123 0.042 0.012 0.018 0.003 99.88 7.73 0.007 0.393 0.009 0.043 1.214 0.054 3.607 1.942 0.059 0.022 0.019 0.003 15.081 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph2_pt1 41.74 0.449 16.63 0.015 15.81 0.258 9.01 11.54 2.24 0.475 0 0.233 0 0.053 100.442 6.127 0.05 2.877 0.002 0.412 1.529 0.032 1.972 1.815 0.638 0.089 0 0.058 15.541 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph2_pt2 41.75 0.324 16.59 0 15.65 0.259 9.1 11.75 2.23 0.441 0.022 0.231 0.009 0.052 100.341 6.138 0.036 2.875 0 0.357 1.568 0.032 1.995 1.851 0.636 0.083 0.01 0.058 15.569 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph2_pt3 42.15 0.389 15.88 0.006 15.88 0.276 9.46 11.78 2.13 0.451 0.066 0.193 0.028 0.044 100.636 6.172 0.043 2.741 0.001 0.444 1.501 0.034 2.065 1.848 0.605 0.084 0.031 0.048 15.537 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph3_pt1 54.9 0.061 2.41 0 10.05 0.473 17.28 12.79 0.232 0.136 0.149 0 0.063 0 100.452 7.728 0.006 0.4 0 0.185 0.998 0.056 3.626 1.929 0.063 0.024 0.066 0 15.017 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph3_pt2 54 0 2.94 0.017 10.66 0.527 16.66 12.86 0.314 0.185 0.01 0.005 0.004 0.001 100.22 7.657 0 0.491 0.002 0.164 1.1 0.063 3.522 1.954 0.086 0.034 0.005 0.001 15.074 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_027_amph3_pt3 55.39 0.05 1.452 0.034 10.94 0.346 17.14 12.9 0.13 0.054 0 0.005 0 0.001 100.55 7.84 0.005 0.242 0.004 0.019 1.276 0.041 3.617 1.956 0.036 0.01 0 0.001 15.046 Metamorphic T.S. block UDD1510 144.035 2344.07 0.0171 3.325342466M400_028_amph1_pt1 47.66 0.061 8.66 0.042 17.59 0.282 10.07 11.8 0.917 0.185 0 0.001 0 0 99.383 7.048 0.007 1.509 0.005 0.339 1.837 0.035 2.22 1.87 0.263 0.035 0 0 15.167 Metamorphic T.S. block UDD1510 158.067 2322.17 0.0907 11.20567376M400_028_amph1_pt2 48.56 0.134 7.34 0.013 17.43 0.271 11.25 11.69 0.772 0.1 0.007 0.011 0.003 0.002 99.69 7.182 0.015 1.279 0.002 0.085 2.07 0.034 2.48 1.852 0.221 0.019 0.003 0.003 15.24 Metamorphic T.S. block UDD1510 158.067 2322.17 0.0907 11.20567376M400_028_amph1_pt3 48.33 0.008 7.63 0.032 18.16 0.269 10.91 11.93 0.857 0.109 0 0.013 0 0.003 100.356 7.12 0.001 1.325 0.004 0.164 2.073 0.034 2.396 1.883 0.245 0.02 0 0.003 15.265 Metamorphic T.S. block UDD1510 158.067 2322.17 0.0907 11.20567376M400_041_amph1_pt2 41.89 0.54 13.4 0.254 22.07 0.407 5.33 11.52 1.47 0.382 0 0.029 0 0.006 99.373 6.336 0.061 2.389 0.03 0.82 1.972 0.052 1.202 1.867 0.431 0.074 0 0.007 15.235 Al-amphibole T.S. block PERCD8151A 387.969 2335.49 0.0142M400_041_amph1_pt3 41.38 0.775 13.66 0.375 22.44 0.336 5.43 11.78 1.49 0.496 0 0.006 0 0.001 100.275 6.218 0.088 2.419 0.044 0.906 1.914 0.043 1.216 1.897 0.434 0.095 0 0.001 15.274 Al-amphibole T.S. block PERCD8151A 387.969 2335.49 0.0142M400_041_amph1_pt3 42.08 0.563 13.49 0.225 21.98 0.369 5.54 11.68 1.47 0.417 0.016 0.019 0.007 0.004 99.954 6.326 0.064 2.39 0.027 0.818 1.945 0.047 1.242 1.881 0.428 0.08 0.007 0.005 15.248 Al-amphibole T.S. block PERCD8151A 387.969 2335.49 0.0142M400_041_amph2_pt1 41.22 0.419 14.23 0.209 22.75 0.245 5.07 11.68 1.55 0.41 0 0.015 0 0.003 99.899 6.21 0.047 2.527 0.025 0.941 1.925 0.031 1.139 1.885 0.453 0.079 0 0.004 15.262 Al-amphibole T.S. block PERCD8151A 387.969 2335.49 0.0142M400_041_amph2_pt2 40.25 0.287 15.82 0.258 22.29 0.261 4.53 11.64 1.57 0.433 0 0.018 0 0.004 99.466 6.086 0.033 2.819 0.031 0.915 1.904 0.033 1.021 1.886 0.46 0.084 0 0.004 15.271 Al-amphibole T.S. block PERCD8151A 387.969 2335.49 0.0142M400_041_amph2_pt3 39.61 0.231 16.55 0.253 22.17 0.203 4.4 11.62 1.47 0.617 0 0 0 0 99.101 6.007 0.026 2.958 0.03 0.912 1.899 0.026 0.995 1.888 0.432 0.119 0 0 15.293 Al-amphibole T.S. block PERCD8151A 387.969 2335.49 0.0142M400_043_amph1_pt1 56.2 0 0.397 0.068 6.23 0.122 21.05 12.76 0.132 0.007 0 0 0 0 99.106 7.872 0 0.065 0.008 0.145 0.584 0.014 4.396 1.915 0.036 0.001 0 0 15.037 Metamorphic T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_amph1_pt2 56.07 0.023 0.525 0.103 7.19 0.123 20.68 12.66 0.141 0.021 0 0.001 0 0 99.676 7.839 0.002 0.086 0.011 0.178 0.662 0.015 4.31 1.896 0.038 0.004 0 0 15.042 Metamorphic T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_amph1_pt3 56.34 0 0.374 0.088 6.7 0.122 20.85 12.29 0.146 0.009 0.021 0 0.009 0 99.048 7.912 0 0.062 0.01 0.062 0.725 0.014 4.365 1.849 0.04 0.002 0.009 0 15.041 Metamorphic T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_amph2_pt1 56.73 0.015 0.163 0.001 6.06 0.128 21.55 12.76 0.054 0.004 0 0 0 0 99.624 7.882 0.002 0.027 0 0.205 0.499 0.015 4.464 1.899 0.015 0.001 0 0 15.008 Si-amphibole T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_amph2_pt2 56.69 0.004 0.182 0.033 5.73 0.12 21.49 12.75 0.059 0 0 0.003 0 0.001 99.218 7.904 0 0.03 0.004 0.157 0.511 0.014 4.467 1.905 0.016 0 0 0.001 15.008 Si-amphibole T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_amph2_pt3 56.78 0.011 0.333 0.091 5.63 0.133 21.86 12.5 0.166 0.001 0.017 0 0.007 0 99.631 7.87 0.001 0.054 0.01 0.192 0.461 0.016 4.517 1.856 0.044 0 0.007 0 15.022 Si-amphibole T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_cum1_pt1 55.42 0.004 0.038 0.016 18.23 0.505 22.31 0.692 0.029 0.008 0 0.003 0 0.001 99.364 7.903 0 0.006 0.002 0.183 1.991 0.061 4.743 0.106 0.008 0.001 0 0.001 15.005 Si-amphibole T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_cum1_pt2 55.58 0 0.055 0.018 18.04 0.483 22.39 0.695 0.022 0 0 0 0 0 99.388 7.917 0 0.009 0.002 0.154 1.995 0.058 4.755 0.106 0.006 0 0 0 15.003 Si-amphibole T.S. block PERCD8151A 410.076 2307.89 0.0247M400_043_cum1_pt3 55.86 0 0.069 0.002 17.5 0.416 23 0.672 0.016 0.002 0 0 0 0 99.655 7.908 0 0.012 0 0.171 1.9 0.05 4.854 0.102 0.005 0 0 0 15.003 Si-amphibole T.S. block PERCD8151A 410.076 2307.89 0.0247
M400_045_amph1_pt1 49.21 0.12 8.55 0.017 12.25 0.246 13.68 12.23 1.1 0.133 0.016 0 0.007 0 99.654 7.089 0.013 1.452 0.002 0.234 1.242 0.03 2.938 1.888 0.307 0.024 0.007 0 15.219 Metamorphic T.S. block PERCD8151A 423.494 2317.69 0.0804 2.723214286M400_045_amph1_pt2 49.83 0.147 8.06 0.1 11.2 0.243 14.37 12.17 0.933 0.104 0 0.015 0 0.003 99.279 7.157 0.016 1.364 0.011 0.255 1.091 0.03 3.077 1.873 0.26 0.019 0 0.004 15.151 Metamorphic T.S. block PERCD8151A 423.494 2317.69 0.0804 2.723214286M400_045_amph1_pt3 48.39 0.275 8.99 0.262 11.89 0.238 13.83 12.23 1.208 0.077 0 0.011 0 0.003 99.513 6.977 0.03 1.528 0.03 0.298 1.136 0.029 2.973 1.889 0.338 0.014 0 0.003 15.241 Metamorphic T.S. block PERCD8151A 423.494 2317.69 0.0804 2.723214286M400_045_amph2_pt1 52.98 0.132 4.39 0.058 10.43 0.227 16.66 12.56 0.547 0.053 0 0.002 0 0 100.153 7.482 0.014 0.731 0.006 0.31 0.922 0.027 3.508 1.9 0.15 0.009 0 0 15.06 Metamorphic T.S. block PERCD8151A 423.494 2317.69 0.0804 2.723214286
M400_047Amph1p1 41.8 0.176 16.6 0.012 19.75 0.4 5.68 11.57 1.285 0.545 0 0.081 0 0.018 99.99 6.211 0.02 2.907 0.001 0.668 1.787 0.05 1.258 1.842 0.37 0.103 0 0.02 15.218 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph1p2 42.13 0.216 16.37 0 20 0.447 5.75 11.42 1.45 0.418 0.04 0.062 0.017 0.014 100.367 6.227 0.024 2.851 0 0.742 1.73 0.056 1.267 1.808 0.416 0.079 0.019 0.015 15.2 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph1p3 41.86 0.285 15.32 0.362 19.34 0.425 5.65 11.56 1.177 0.621 0 0.033 0 0.007 98.707 6.325 0.032 2.728 0.043 0.505 1.939 0.054 1.273 1.872 0.345 0.12 0 0.008 15.236 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph2p1 41.38 0.546 14.02 0.074 22.55 0.354 5.31 11.35 1.149 0.883 0 0.005 0 0.001 99.729 6.256 0.062 2.498 0.009 0.833 2.018 0.045 1.197 1.839 0.337 0.17 0 0.001 15.265 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph2p2 41.22 0.484 14.07 0.071 22.31 0.399 5.3 11.57 1.171 1.089 0 0.008 0 0.002 99.807 6.246 0.055 2.513 0.009 0.77 2.057 0.051 1.197 1.878 0.344 0.211 0 0.002 15.331 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph2p3 41.57 0.455 13.7 0.064 22.82 0.413 5.38 11.54 1.153 1.168 0.03 0.001 0.012 0 100.396 6.271 0.052 2.436 0.008 0.807 2.072 0.053 1.21 1.865 0.337 0.225 0.014 0 15.334 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph3p1 41.44 0.212 16.41 0.131 19.83 0.367 5.29 11.44 1.314 0.666 0.032 0.064 0.014 0.014 99.27 6.227 0.024 2.906 0.016 0.589 1.903 0.047 1.185 1.842 0.383 0.128 0.015 0.016 15.249 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph3p2 41.97 0.238 16.26 0.011 19.57 0.354 5.78 11.44 1.33 0.597 0.035 0.044 0.015 0.01 99.688 6.253 0.027 2.855 0.001 0.628 1.811 0.045 1.284 1.826 0.384 0.113 0.016 0.011 15.227 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_047Amph3p3 42.67 0.293 15.63 0.002 19.75 0.36 6.17 11.39 1.337 0.558 0 0.051 0 0.012 100.288 6.309 0.033 2.724 0 0.668 1.775 0.045 1.36 1.804 0.383 0.105 0 0.013 15.207 Al-amphibole T.S. block PERCD8151A 428.911 2344.88 0.0115 3.965517241M400_054Amph1p1 41.67 0.103 15.26 0.558 18.68 0.283 7.29 11.86 1.54 0.143 0 0.015 0 0.003 99.503 6.163 0.011 2.66 0.065 0.993 1.317 0.035 1.607 1.879 0.442 0.027 0 0.004 15.201 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph1p2 41.9 0.031 15.03 0.469 18.58 0.335 7.66 11.75 1.57 0.115 0 0.013 0 0.003 99.563 6.176 0.003 2.611 0.055 1.073 1.217 0.042 1.683 1.856 0.449 0.022 0 0.003 15.186 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph1p3 41.78 0.034 15.31 0.539 18.36 0.32 7.48 11.56 1.54 0.13 0 0.006 0 0.001 99.172 6.179 0.004 2.669 0.063 1.024 1.246 0.04 1.649 1.832 0.442 0.025 0 0.002 15.172 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph2p1 53.53 0.016 2.54 0.553 13.79 0.247 14.15 12.44 0.193 0.029 0 0.002 0 0 99.591 7.749 0.002 0.433 0.063 0.085 1.585 0.03 3.053 1.929 0.054 0.005 0 0.001 14.989 Metamorphic HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph2p2 53.94 0 2.44 0.468 13.54 0.216 14.43 12.71 0.196 0.035 0 0 0 0 100.055 7.774 0 0.414 0.053 0 1.632 0.026 3.1 1.963 0.055 0.006 0 0 15.024 Metamorphic HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph2p3 53.3 0.062 2.46 0.643 13.66 0.273 14.22 12.45 0.224 0.025 0 0 0 0 99.383 7.733 0.007 0.421 0.074 0.089 1.568 0.034 3.075 1.935 0.063 0.005 0 0 15.003 Metamorphic HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph3p1 43.8 0.034 12.74 0.003 18.34 0.268 8.22 11.88 1.145 0.116 0 0.017 0 0.004 98.675 6.518 0.004 2.234 0 0.787 1.495 0.034 1.824 1.894 0.33 0.022 0 0.004 15.143 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph5p1 42.65 0 14.97 0.039 20.64 0.362 6.97 11.64 1.51 0.108 0 0.022 0 0.005 101.019 6.225 0 2.575 0.004 1.109 1.41 0.045 1.517 1.82 0.427 0.02 0 0.005 15.154 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph5p2 41.9 0.045 15.29 0.001 20.8 0.354 6.93 11.62 1.69 0.105 0 0 0 0 100.786 6.126 0.005 2.635 0 1.24 1.303 0.044 1.51 1.82 0.479 0.02 0 0 15.181 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_054Amph5p3 41.72 0.004 15.88 0.001 20.95 0.366 6.73 11.6 1.8 0.113 0 0.012 0 0.003 101.224 6.073 0 2.725 0 1.271 1.279 0.045 1.461 1.809 0.508 0.021 0 0.003 15.193 Al-amphibole HyChips-RC LARCD1027 278-279 2330.48 0.0263 3.043478261M400_060Amph1p1 49.47 0.02 5.44 0.011 21.95 0.295 8.34 11.81 0.667 0.266 0 0.012 0 0.003 100.392 7.376 0.002 0.956 0.001 0.343 2.394 0.037 1.854 1.887 0.193 0.051 0 0.003 15.093 Si-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph1p2 51.23 0.004 3.57 0 23.06 0.294 9.3 11.82 0.435 0.216 0 0.006 0 0.001 102.048 7.54 0 0.619 0 0.26 2.579 0.037 2.04 1.864 0.124 0.041 0 0.002 15.103 Si-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph1p3 51.94 0 2.86 0.016 22.31 0.308 9.25 11.95 0.327 0.156 0 0.008 0 0.002 101.239 7.674 0 0.498 0.002 0.232 2.525 0.039 2.037 1.892 0.094 0.029 0 0.002 15.021 Si-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph2p1 41.62 0.046 12.93 0 25.86 0.286 4.42 11.43 1.4 0.671 0.018 0.064 0.008 0.015 100.806 6.281 0.005 2.3 0 1.129 2.135 0.036 0.994 1.848 0.41 0.129 0.009 0.016 15.269 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph2p2 41.42 0.042 13.24 0.006 25.64 0.297 4.3 11.48 1.35 0.648 0 0.074 0 0.017 100.571 6.265 0.005 2.36 0.001 1.093 2.151 0.038 0.97 1.86 0.396 0.125 0 0.019 15.263 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph2p3 40.88 0.108 13.37 0.03 26.17 0.309 4.02 11.54 1.36 0.649 0.008 0.068 0.003 0.015 100.59 6.222 0.012 2.398 0.004 0.997 2.334 0.04 0.912 1.882 0.401 0.126 0.004 0.018 15.329 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph3p1 40.79 0 14.69 0.011 25.17 0.266 4.12 11.62 1.4 0.576 0.023 0.025 0.01 0.006 100.771 6.138 0 2.605 0.001 1.11 2.058 0.034 0.924 1.873 0.408 0.111 0.011 0.006 15.263 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph3p2 41.82 0.054 11.61 0 24.84 0.225 5.08 11.58 1.35 0.743 0 0.078 0 0.018 99.461 6.398 0.006 2.093 0 1.031 2.147 0.029 1.159 1.898 0.4 0.145 0 0.02 15.306 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph4p2 52.18 0.016 2.82 0 20.74 0.308 10.29 11.71 0.393 0.168 0 0.013 0 0.003 100.75 7.68 0.002 0.489 0 0.273 2.28 0.038 2.258 1.847 0.112 0.032 0 0.003 15.009 Si-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438
A-3
M400_060Amph4p3 50.95 0.016 4.02 0 20.92 0.311 9.77 11.81 0.506 0.189 0 0.011 0 0.002 100.612 7.521 0.002 0.699 0 0.35 2.233 0.039 2.15 1.868 0.145 0.035 0 0.003 15.042 Si-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph5p1 46.26 0.361 5.42 0.015 26.53 0.475 7.09 9.96 0.768 0.714 0 0.238 0 0.054 99.843 7.171 0.042 0.99 0.002 0.209 3.23 0.062 1.639 1.654 0.231 0.141 0 0.062 15.372 Metamorphic HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph5p2 45.14 0.211 6.48 0.005 27.45 0.437 5.74 10.69 1.013 0.901 0 0.383 0 0.086 100.414 7.033 0.025 1.19 0.001 0.209 3.367 0.058 1.333 1.784 0.306 0.179 0 0.101 15.485 Metamorphic HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph5p3 45.3 0.184 6.13 0.008 26.56 0.478 6.21 10.5 1.005 0.838 0 0.384 0 0.087 99.522 7.093 0.022 1.131 0.001 0.165 3.313 0.063 1.45 1.762 0.305 0.167 0 0.102 15.473 Metamorphic HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph6p1 40.32 0.1 13.81 0 24.75 0.325 3.95 11.63 1.38 0.559 0 0.036 0 0.008 98.948 6.202 0.012 2.504 0 1.015 2.169 0.042 0.906 1.917 0.412 0.11 0 0.009 15.287 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph6p2 40.41 0.031 14.18 0 24.82 0.279 4.19 11.46 1.37 0.569 0.003 0.025 0.001 0.006 99.437 6.164 0.004 2.549 0 1.109 2.057 0.036 0.953 1.873 0.405 0.111 0.001 0.007 15.261 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_060Amph6p3 41.2 0.039 13.74 0 24.47 0.312 4.28 11.41 1.44 0.535 0 0.031 0 0.007 99.558 6.272 0.004 2.465 0 0.993 2.122 0.04 0.971 1.861 0.425 0.104 0 0.008 15.259 Al-amphibole HyChips-RC LARCD1011 83-84 2342.04 NULL 3.335616438M400_062Amph1p1 41.94 0.1 12.8 0 24.71 0.277 5.16 11.53 1.36 0.67 0.061 0.045 0.026 0.01 100.732 6.305 0.011 2.268 0 1.092 2.015 0.035 1.156 1.857 0.396 0.129 0.029 0.012 15.266 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph1p2 41.8 0.077 12.5 0 24.94 0.294 4.79 11.55 1.47 0.653 0 0.1 0 0.023 100.225 6.336 0.009 2.233 0 1.051 2.111 0.038 1.082 1.876 0.432 0.126 0 0.026 15.293 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph1p3 41.81 0.092 12.97 0.017 25.21 0.281 4.84 11.66 1.38 0.557 0.015 0.063 0.006 0.014 100.965 6.279 0.01 2.296 0.002 1.118 2.048 0.036 1.084 1.876 0.402 0.107 0.007 0.016 15.257 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph2p1 50.62 0 4.27 0.012 21.47 0.301 9.69 11.76 0.556 0.139 0 0.015 0 0.003 100.945 7.484 0 0.744 0.001 0.259 2.396 0.038 2.136 1.863 0.159 0.026 0 0.004 15.106 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph2p2 53.44 0 2.08 0.014 19.22 0.278 11.45 11.97 0.267 0.061 0 0.001 0 0 100.892 7.796 0 0.358 0.002 0.17 2.175 0.034 2.49 1.871 0.075 0.011 0 0 14.983 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph2p3 51.14 0.023 4.21 0 19.83 0.314 9.98 11.84 0.456 0.111 0 0.001 0 0 100.023 7.566 0.003 0.734 0 0.231 2.223 0.039 2.201 1.877 0.131 0.021 0 0 15.025 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph2p4 51.81 0 3.26 0.011 20.25 0.298 10.53 11.83 0.386 0.121 0 0 0 0 100.527 7.65 0 0.567 0.001 0.109 2.391 0.037 2.318 1.871 0.11 0.023 0 0 15.078 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph3p1 45.5 0.298 6.21 0.004 25.55 0.325 6.79 10.37 0.787 0.82 0.023 0.176 0.01 0.04 98.892 7.115 0.035 1.145 0 0.152 3.189 0.043 1.583 1.737 0.239 0.164 0.011 0.047 15.402 Metamorphic HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph3p2 46.71 0.172 5.62 0 25.3 0.246 7.47 10.18 0.988 0.698 0 0.159 0 0.036 99.563 7.233 0.02 1.026 0 0.035 3.242 0.032 1.724 1.689 0.297 0.138 0 0.042 15.434 Metamorphic HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph3p3 45.78 0.221 5.99 0.009 26.2 0.294 7.04 9.86 0.896 0.754 0.093 0.152 0.039 0.034 99.288 7.136 0.026 1.1 0.001 0.154 3.261 0.039 1.636 1.647 0.271 0.15 0.046 0.04 15.421 Metamorphic HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph4p1 51.45 0 2.53 0.016 21.67 0.426 9.89 10.83 0.369 0.253 0.011 0.057 0.004 0.013 99.514 7.746 0 0.449 0.002 0.008 2.72 0.054 2.22 1.747 0.108 0.049 0.005 0.014 15.103 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph4p2 51.22 0.073 2.41 0 23.44 0.537 10.13 9.94 0.419 0.238 0.034 0.055 0.014 0.012 100.565 7.658 0.008 0.425 0 0.197 2.733 0.068 2.258 1.592 0.121 0.045 0.016 0.014 15.106 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph4p3 50.8 0.084 2.66 0 23.96 0.505 9.69 9.76 0.371 0.257 0.031 0.082 0.013 0.019 100.254 7.641 0.01 0.472 0 0.178 2.836 0.064 2.173 1.573 0.108 0.049 0.015 0.021 15.103 Si-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph5p1 40.89 0 13.67 0.015 24.69 0.248 4.44 11.35 1.35 0.569 0.059 0.058 0.025 0.013 99.394 6.235 0 2.457 0.002 1.086 2.063 0.032 1.009 1.854 0.399 0.111 0.028 0.015 15.248 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph5p2 40.57 0.031 14.24 0.006 24.94 0.237 4.05 11.47 1.44 0.482 0 0.028 0 0.006 99.558 6.178 0.004 2.556 0.001 1.091 2.085 0.031 0.919 1.871 0.425 0.094 0 0.007 15.254 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph5p3 40.88 0.054 14.5 0.024 24.63 0.275 4.3 11.44 1.41 0.503 0 0.042 0 0.009 100.157 6.174 0.006 2.581 0.003 1.086 2.025 0.035 0.968 1.851 0.413 0.097 0 0.011 15.24 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph6p1 40.29 0.05 14.54 0.008 26.68 0.391 3.42 11.51 1.36 0.607 0 0.062 0 0.014 101.01 6.114 0.006 2.6 0.001 1.036 2.35 0.05 0.774 1.871 0.4 0.117 0 0.016 15.32 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph6p2 40.34 0 14.37 0.015 26.19 0.339 3.47 11.53 1.36 0.682 0 0.074 0 0.017 100.454 6.134 0 2.575 0.002 1.122 2.209 0.044 0.787 1.878 0.401 0.132 0 0.019 15.283 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_062Amph6p3 39.98 0.084 14.78 0 26.18 0.353 3.32 11.57 1.319 0.71 0.071 0.062 0.03 0.014 100.483 6.083 0.01 2.651 0 1.117 2.214 0.046 0.753 1.886 0.389 0.138 0.034 0.016 15.287 Al-amphibole HyChips-RC LARCD1011 123-124 2339.59 0.0112 4.714640199M400_064Amph1p1 41.64 0.061 14.54 0.006 26.12 0.311 3.71 11.44 1.37 0.31 0 0.027 0 0.006 101.594 6.244 0.007 2.57 0.001 0.863 2.412 0.04 0.829 1.838 0.398 0.059 0 0.007 15.261 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph1p2 41.68 0.046 14.06 0.011 26.1 0.248 3.9 11.45 1.346 0.258 0 0.021 0 0.005 101.225 6.271 0.005 2.493 0.001 0.899 2.385 0.032 0.875 1.846 0.393 0.05 0 0.005 15.248 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph1p3 41.23 0.034 15.19 0 25.47 0.282 3.71 11.43 1.35 0.264 0.054 0.011 0.023 0.003 101.112 6.199 0.004 2.692 0 0.847 2.356 0.036 0.832 1.841 0.394 0.051 0.025 0.003 15.25 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph2p1 50.87 0 4.14 0.02 23.2 0.293 8.68 11.58 0.553 0.096 0.031 0.023 0.013 0.005 101.494 7.573 0 0.726 0.002 0 2.888 0.037 1.926 1.847 0.16 0.018 0.015 0.006 15.178 Metamorphic HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph2p2 49.13 0.027 5.97 0.023 23.29 0.274 7.76 11.77 0.723 0.118 0 0.027 0 0.006 101.203 7.301 0.003 1.046 0.003 0.365 2.529 0.034 1.719 1.874 0.208 0.022 0 0.007 15.105 Metamorphic HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph2p3 48.11 0.062 6.71 0 24.11 0.305 7.57 11.4 0.77 0.188 0.023 0.028 0.01 0.006 101.369 7.218 0.007 1.186 0 0.105 2.92 0.039 1.693 1.832 0.224 0.036 0.011 0.007 15.26 Metamorphic HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph3p1 46.22 0.115 6.32 0 26.35 0.31 7.21 10.37 0.879 0.392 0 0.254 0 0.057 100.46 7.081 0.013 1.141 0 0.333 3.043 0.04 1.647 1.702 0.261 0.077 0 0.066 15.338 Metamorphic HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph3p2 46.28 0.245 6.12 0 26.17 0.351 7.35 10.37 0.882 0.369 0 0.267 0 0.06 100.391 7.089 0.028 1.105 0 0.327 3.025 0.045 1.678 1.702 0.262 0.072 0 0.069 15.334 Metamorphic HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph3p3 47.27 0.188 5.67 0.008 26.34 0.341 7.16 9.97 0.784 0.355 0.051 0.196 0.021 0.044 100.31 7.252 0.022 1.025 0.001 0.124 3.256 0.044 1.638 1.639 0.233 0.07 0.025 0.051 15.303 Metamorphic HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph4p1 41.7 0.031 13.78 0.01 25.88 0.291 3.86 11.42 1.36 0.567 0 0.024 0 0.005 101.005 6.278 0.003 2.445 0.001 1.02 2.238 0.037 0.866 1.842 0.397 0.109 0 0.006 15.238 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph4p2 42.16 0.038 13.17 0.008 26.45 0.308 3.86 11.44 1.331 0.629 0 0.047 0 0.011 101.542 6.332 0.004 2.331 0.001 1.015 2.308 0.039 0.864 1.841 0.387 0.121 0 0.012 15.244 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph4p3 40.97 0 15.11 0 26.26 0.287 3.32 11.36 1.38 0.731 0.048 0.067 0.02 0.015 101.604 6.148 0 2.672 0 1.047 2.248 0.037 0.743 1.826 0.402 0.14 0.023 0.017 15.263 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph5p1 40.44 0.035 15.61 0.008 26.51 0.308 2.57 11.45 1.37 0.716 0.015 0.035 0.006 0.008 101.127 6.119 0.004 2.784 0.001 0.954 2.4 0.04 0.58 1.856 0.402 0.138 0.007 0.009 15.278 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph5p2 40.19 0.115 15.57 0.004 26.81 0.326 2.56 11.43 1.37 0.636 0.036 0.053 0.015 0.012 101.173 6.081 0.013 2.777 0 1.039 2.354 0.042 0.577 1.853 0.402 0.123 0.017 0.014 15.26 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_064Amph5p3 39.54 0 15.21 0.012 27.21 0.291 2.66 11.3 1.41 0.915 0.041 0.088 0.017 0.02 100.724 6.031 0 2.734 0.001 1.158 2.313 0.038 0.605 1.847 0.417 0.178 0.02 0.023 15.32 Al-amphibole HyChips-RC LARCD0919 138-139 2336.84 0.0268 6.567656766M400_066Amph1p1 40.84 0.073 13.42 0.028 26.13 0.273 3.82 11.43 1.333 0.603 0 0.048 0 0.011 100.06 6.224 0.008 2.411 0.003 1.116 2.215 0.035 0.868 1.866 0.394 0.117 0 0.012 15.258 Al-amphibole HyChips-RC LARCD0920 119-120 2354.16 NULL 1.982651797M400_066Amph1p2 40.17 0.061 13.66 0 27.45 0.252 3.32 11.42 1.281 0.741 0.041 0.07 0.017 0.016 100.536 6.155 0.007 2.467 0 1.059 2.458 0.033 0.758 1.875 0.38 0.145 0.02 0.018 15.338 Al-amphibole HyChips-RC LARCD0920 119-120 2355.16 NULL 1.982651797M400_066Amph1p3 39.83 0.08 13.63 0.006 27.32 0.246 3.1 11.43 1.36 0.858 0 0.097 0 0.022 100.013 6.128 0.009 2.471 0.001 1.178 2.337 0.032 0.711 1.884 0.406 0.168 0 0.025 15.325 Al-amphibole HyChips-RC LARCD0920 119-120 2356.16 NULL 1.982651797M400_071Amph2p1 55.61 0.015 1.328 0.056 10.32 0.199 16.82 12.86 0.111 0.002 0.008 0 0.004 0 99.405 7.936 0.002 0.223 0.006 0 1.232 0.024 3.578 1.966 0.031 0 0.004 0 14.999 Si-amphibole T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph2p2 55.95 0 1.241 0.042 10.31 0.219 16.83 13.07 0.102 0.049 0.085 0 0.036 0 99.975 7.957 0 0.208 0.005 0 1.226 0.026 3.568 1.992 0.028 0.009 0.038 0 15.019 Si-amphibole T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph2p3 55.72 0.062 1.163 0.069 10.42 0.235 16.73 12.8 0.101 0.029 0 0 0 0 99.427 7.96 0.007 0.196 0.008 0 1.245 0.028 3.563 1.959 0.028 0.005 0 0 14.998 Si-amphibole T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph3p1 49.96 0.023 4.5 0.053 16.93 0.363 13.78 10.98 0.611 0.482 0 0.053 0 0.012 99.76 7.34 0.003 0.779 0.006 0.265 1.815 0.045 3.018 1.728 0.174 0.09 0 0.013 15.264 Metamorphic T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph3p2 49.84 0 4.75 0.083 16.99 0.327 13.33 11.21 0.638 0.501 0.039 0.06 0.016 0.013 99.84 7.339 0 0.824 0.01 0.213 1.88 0.041 2.926 1.768 0.182 0.094 0.018 0.015 15.276 Metamorphic T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph3p3 49.25 0.081 5.09 0.103 17.02 0.307 13.28 11.18 0.667 0.511 0.028 0.066 0.012 0.015 99.638 7.267 0.009 0.885 0.012 0.264 1.836 0.038 2.921 1.767 0.191 0.096 0.013 0.016 15.287 Metamorphic T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph4p1 53.47 0 3.43 0 13.16 0.245 14.27 12.92 0.199 0.094 0 0 0 0 99.868 7.709 0 0.583 0 0 1.587 0.03 3.067 1.996 0.056 0.017 0 0 15.045 Si-amphibole T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph4p2 53.99 0 3.55 0 13.11 0.229 14.28 12.88 0.262 0.089 0.023 0 0.009 0 100.484 7.732 0 0.599 0 0 1.57 0.028 3.049 1.976 0.073 0.016 0.01 0 15.043 Si-amphibole T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_071Amph4p3 53.56 0 3.15 0 13.05 0.223 14.69 12.92 0.198 0.098 0 0.001 0 0 99.997 7.7 0 0.534 0 0.054 1.515 0.027 3.149 1.99 0.055 0.018 0 0 15.042 Si-amphibole T.S. block LNGT001 117.1 2316.06 0.0375 1.797619048M400_073Amph1p1 55.06 0.019 2.25 0.055 10.92 0.247 16.4 12.78 0.284 0.032 0.04 0 0.017 0 100.187 7.812 0.002 0.376 0.006 0.04 1.256 0.03 3.469 1.943 0.078 0.006 0.018 0 15.017 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph1p2 56.54 0 0.902 0.056 11.18 0.25 16.7 12.67 0.128 0.018 0.005 0.003 0.002 0.001 100.547 7.993 0 0.15 0.006 0 1.322 0.03 3.52 1.919 0.035 0.003 0.002 0.001 14.979 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph1p3 54.82 0.061 2.62 0.026 10.92 0.273 16.25 12.67 0.214 0.055 0.107 0.009 0.045 0.002 100.093 7.787 0.007 0.439 0.003 0.034 1.263 0.033 3.441 1.928 0.059 0.01 0.048 0.002 15.003 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph2p1 54.87 0.031 2.59 0.31 11.7 0.222 16.07 12.58 0.293 0.056 0 0.03 0 0.007 100.808 7.748 0.003 0.431 0.035 0.12 1.262 0.027 3.383 1.903 0.08 0.01 0 0.007 15.001 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph2p2 54.74 0 2.22 0.164 12.2 0.334 15.84 12.71 0.239 0.042 0 0 0 0 100.602 7.77 0 0.371 0.018 0.129 1.319 0.04 3.352 1.933 0.066 0.008 0 0 15.007 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph2p3 54.85 0.057 2.57 0.123 11.64 0.299 15.79 12.6 0.292 0.031 0 0.012 0 0.003 100.374 7.79 0.006 0.43 0.014 0.042 1.341 0.036 3.343 1.917 0.08 0.006 0 0.003 15.004 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph3p1 49.61 0.027 7.48 0 14.72 0.285 12.37 12.08 0.778 0.074 0.013 0.009 0.005 0.002 99.523 7.211 0.003 1.281 0 0.295 1.494 0.035 2.68 1.881 0.219 0.014 0.006 0.002 15.114 Metamorphic T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph3p2 50.45 0.091 7.08 0.017 14.5 0.286 12.73 12.34 0.647 0.076 0.073 0 0.031 0 100.369 7.269 0.01 1.202 0.002 0.233 1.514 0.035 2.734 1.905 0.181 0.014 0.033 0 15.1 Metamorphic T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph3p3 50.16 0.102 6.98 0.017 15.05 0.292 12.56 12.15 0.748 0.064 0 0.008 0 0.002 100.211 7.243 0.011 1.188 0.002 0.322 1.495 0.036 2.704 1.88 0.21 0.012 0 0.002 15.101 Metamorphic T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph4p1 50.55 0.125 4.5 0.031 18.65 0.393 11.32 11.11 0.829 0.182 0 0.155 0 0.035 99.925 7.402 0.014 0.777 0.004 0.632 1.652 0.049 2.471 1.743 0.235 0.034 0 0.038 15.012 Metamorphic T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph4p2 46.51 0.234 7.97 0.083 19.96 0.309 9.4 11.63 1.082 0.469 0 0.279 0 0.063 99.94 6.941 0.026 1.402 0.01 0.533 1.958 0.039 2.091 1.86 0.313 0.089 0 0.07 15.262 Metamorphic T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph4p3 47.78 0.257 6.48 0.011 19.72 0.328 9.74 11.44 0.946 0.384 0 0.244 0 0.055 99.318 7.147 0.029 1.142 0.001 0.49 1.977 0.042 2.172 1.833 0.274 0.073 0 0.062 15.181 Metamorphic T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph5p1 55.67 0.016 2.1 0.07 11.27 0.219 16.59 12.57 0.172 0.015 0 0 0 0 100.823 7.835 0.002 0.348 0.008 0.075 1.251 0.026 3.481 1.896 0.047 0.003 0 0 14.972 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph5p2 56.24 0.016 1.563 0.034 10.55 0.272 16.84 12.77 0.195 0.026 0 0.005 0 0.001 100.639 7.928 0.002 0.26 0.004 0 1.244 0.033 3.539 1.929 0.053 0.005 0 0.001 14.995 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_073Amph5p3 55.9 0 1.791 0.058 11.36 0.245 16.53 12.95 0.111 0.02 0 0 0 0 101.095 7.869 0 0.297 0.006 0.003 1.334 0.029 3.469 1.953 0.03 0.004 0 0 14.995 Si-amphibole T.S. block LNGT001 172.15 2336.89 0.0143 2.835249042M400_082Amph1p1 57.22 0 1.273 0.556 7.73 0.179 19.03 11.33 1.47 0.07 0 0.007 0 0.002 100.914 7.901 0 0.207 0.061 0.171 0.721 0.021 3.917 1.676 0.394 0.012 0 0.002 15.082 Metamorphic T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph1p2 57.69 0 1.185 0.634 7.44 0.191 19.05 10.98 1.63 0.095 0.056 0.006 0.024 0.001 101.049 7.947 0 0.192 0.069 0.151 0.706 0.022 3.912 1.621 0.435 0.017 0.025 0.001 15.073 Metamorphic T.S. block DUDH0130 129.8 2312.95 0.0233
A-4
M400_082Amph1p3 57.14 0.065 1.211 0.484 7.66 0.153 19.39 11.61 1.185 0.061 0.003 0 0.001 0 101.05 7.866 0.007 0.196 0.053 0.255 0.627 0.018 3.979 1.712 0.316 0.011 0.001 0 15.039 Metamorphic T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph2p1 58.26 0.031 0.468 0.102 7.21 0.258 19.59 12.56 0.46 0.094 0.076 0 0.032 0 101.193 8 0.003 0.076 0.011 0.008 0.82 0.03 4.01 1.848 0.122 0.016 0.033 0 14.945 Metamorphic T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph2p3 57.15 0.054 1.201 0.096 8.3 0.291 19.05 11.15 1.45 0.104 0.037 0 0.016 0 100.949 7.881 0.006 0.195 0.01 0.32 0.637 0.034 3.916 1.647 0.388 0.018 0.016 0 15.053 Metamorphic T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph3p1 58.4 0.023 0.752 0 4.99 0.219 22.2 10.83 1.208 0.31 0.043 0.01 0.018 0.002 101.094 7.88 0.002 0.12 0 0.505 0.058 0.025 4.465 1.566 0.316 0.053 0.018 0.002 14.99 Si-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph3p2 58.27 0.019 0.726 0.02 5.1 0.276 22.38 10.81 0.852 0.272 0.135 0 0.057 0 100.899 7.868 0.002 0.115 0.002 0.546 0.03 0.032 4.505 1.564 0.223 0.047 0.058 0 14.934 Si-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph3p3 58.7 0.027 0.561 0.008 4.95 0.248 21.87 11.23 0.83 0.21 0.127 0 0.054 0 100.765 7.963 0.003 0.09 0.001 0.318 0.243 0.029 4.423 1.632 0.218 0.036 0.055 0 14.957 Si-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph4p1 47.15 0.216 8.67 0.217 12.43 0.212 14.79 11.23 2.21 0.736 0.156 0.009 0.066 0.002 100.049 6.709 0.023 1.454 0.024 1.185 0.294 0.026 3.137 1.712 0.61 0.134 0.07 0.002 15.308 Al-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph4p2 45.75 0.254 9.47 0.203 12.39 0.168 14.01 11.28 2.31 0.802 0.127 0.005 0.054 0.001 98.755 6.616 0.028 1.614 0.023 1.147 0.351 0.021 3.02 1.748 0.648 0.148 0.058 0.001 15.363 Al-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph4p3 44.95 0.298 9.85 0.062 14.18 0.265 13.4 11.15 2.48 0.816 0.118 0.009 0.05 0.002 99.58 6.478 0.032 1.673 0.007 1.392 0.317 0.032 2.879 1.722 0.693 0.15 0.054 0.002 15.375 Al-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph5p1 57.08 0.034 0.882 0.047 8.71 0.201 18.32 11.65 0.99 0.064 0 0 0 0 100.123 7.98 0.004 0.145 0.005 0.126 0.893 0.024 3.818 1.745 0.268 0.011 0 0 15.019 Si-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph5p2 57.15 0.019 0.831 0.051 9.06 0.154 18.31 11.61 1.068 0.051 0.019 0.009 0.008 0.002 100.468 7.966 0.002 0.137 0.006 0.177 0.879 0.018 3.805 1.734 0.289 0.009 0.008 0.002 15.021 Si-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_082Amph5p3 57.26 0.05 0.868 0.118 9.3 0.195 18.07 11.81 1.089 0.049 0 0 0 0 100.965 7.964 0.005 0.142 0.013 0.135 0.947 0.023 3.746 1.76 0.294 0.009 0 0 15.037 Si-amphibole T.S. block DUDH0130 129.8 2312.95 0.0233M400_083Amph1p1 52.92 0.428 3.54 0.074 11.65 0.404 17.36 10.94 0.669 0.126 0.075 0 0.031 0 100.27 7.549 0.046 0.595 0.008 0 1.39 0.049 3.692 1.672 0.185 0.023 0.034 0 15.208 Metamorphic T.S. block DUDH0130 160 2328.87 NULLM400_083Amph1p2 53.79 0.354 3.21 0.095 11.15 0.387 16.77 11.29 0.59 0.079 0.091 0.013 0.038 0.003 99.859 7.709 0.038 0.542 0.011 0 1.336 0.047 3.583 1.734 0.164 0.014 0.041 0.003 15.178 Metamorphic T.S. block DUDH0130 160 2328.87 NULLM400_083Amph1p3 51.69 0.286 5.32 0.032 11.87 0.422 16.58 10.7 1.008 0.174 0.031 0.003 0.013 0.001 100.173 7.408 0.031 0.899 0.004 0 1.423 0.051 3.542 1.643 0.28 0.032 0.014 0.001 15.312 Metamorphic T.S. block DUDH0130 160 2328.87 NULLM400_083Amph2p1 49.67 0.359 6.69 0 14.94 0.301 13.19 12.13 0.905 0.254 0.028 0.005 0.012 0.001 100.551 7.126 0.039 1.131 0 0.619 1.173 0.037 2.821 1.865 0.252 0.047 0.013 0.001 15.109 Al-amphibole T.S. block DUDH0130 160 2328.87 NULLM400_083Amph2p2 49.02 0.621 7.16 0.022 14.68 0.416 12.99 11.44 1.57 0.313 0.018 0.043 0.008 0.01 100.379 7.036 0.067 1.211 0.002 0.747 1.015 0.051 2.78 1.759 0.437 0.057 0.008 0.011 15.163 Al-amphibole T.S. block DUDH0130 160 2328.87 NULLM400_083Amph2p3 49.04 0.755 7.26 0 13.61 0.399 13.96 11.4 1.345 0.313 0.064 0.015 0.027 0.003 100.228 7 0.081 1.221 0 0.806 0.818 0.048 2.971 1.744 0.372 0.057 0.029 0.004 15.119 Al-amphibole T.S. block DUDH0130 160 2328.87 NULLM400_083Amph3p1 54.69 0.034 0.794 0.104 16.24 0.369 13.7 12.47 0.19 0.062 0 0 0 0 100.729 7.9 0.004 0.135 0.012 0.106 1.856 0.045 2.95 1.93 0.053 0.011 0 0 15.002 Si-amphibole T.S. block DUDH0130 160 2328.87 NULLM400_083Amph3p2 54.28 0.08 0.866 0.15 14.72 0.269 14.44 12.55 0.283 0.049 0.011 0.04 0.004 0.009 99.799 7.872 0.009 0.148 0.017 0.112 1.673 0.033 3.122 1.95 0.08 0.009 0.005 0.01 15.025 Si-amphibole T.S. block DUDH0130 160 2328.87 NULLM400_083Amph3p3 54.16 0.023 0.75 0.177 13.86 0.259 14.57 12.46 0.18 0.029 0 0.011 0 0.002 98.578 7.933 0.003 0.13 0.021 0.018 1.68 0.032 3.181 1.955 0.051 0.005 0 0.003 15.009 Si-amphibole T.S. block DUDH0130 160 2328.87 NULLM400_088Amph1p1 54.63 0 2.48 0.018 11.3 0.143 16.38 12.56 0.331 0.014 0 0 0 0 99.967 7.756 0 0.415 0.002 0.157 1.185 0.017 3.467 1.911 0.091 0.003 0 0 15.003 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph1p2 54.6 0 1.9 0.061 12.2 0.145 15.86 12.95 0.279 0.032 0.03 0 0.013 0 100.155 7.796 0 0.32 0.007 0.09 1.367 0.018 3.376 1.981 0.077 0.006 0.013 0 15.037 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph1p3 51.6 0.031 4.42 0.022 13.15 0.278 14.98 12.39 0.714 0.097 0.12 0 0.051 0 99.855 7.415 0.003 0.749 0.003 0.392 1.188 0.034 3.209 1.908 0.199 0.018 0.055 0 15.118 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph2p1 55.28 0 1.877 0.075 10.23 0.26 17.53 12.06 0.476 0.033 0.033 0.011 0.014 0.003 99.908 7.786 0 0.312 0.008 0.285 0.92 0.031 3.681 1.82 0.13 0.006 0.014 0.003 14.979 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph2p2 55.85 0 1.829 0.103 10.26 0.173 17.14 13 0.261 0.018 0.079 0.001 0.033 0 100.779 7.852 0 0.303 0.011 0.017 1.189 0.021 3.593 1.958 0.071 0.003 0.035 0 15.019 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph2p3 54.12 0.008 2.92 0.033 12.42 0.162 15.72 12.73 0.369 0.01 0 0.005 0 0.001 100.576 7.675 0.001 0.488 0.004 0.218 1.255 0.019 3.323 1.934 0.101 0.002 0 0.001 15.021 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph3p1 47.01 0.046 8.95 0.011 13.99 0.249 13.83 11.87 1.5 0.239 0 0.028 0 0.006 99.833 6.762 0.005 1.517 0.001 0.898 0.785 0.03 2.966 1.829 0.418 0.044 0 0.007 15.256 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph4p1 55.03 0 3.45 0.045 6.55 0.159 19.67 12.77 0.57 0.011 0.083 0.006 0.035 0.001 100.24 7.605 0 0.562 0.005 0.287 0.47 0.019 4.052 1.891 0.153 0.002 0.036 0.001 15.045 Metamorphic T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph4p2 55.77 0.019 1.833 0.394 9.03 0.162 17.65 12.54 0.232 0.015 0.028 0 0.012 0 99.739 7.859 0.002 0.304 0.044 0.078 0.986 0.019 3.708 1.893 0.063 0.003 0.012 0 14.959 Metamorphic T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph4p3 55.4 0 2.1 0.358 8.05 0.192 18.55 12.78 0.326 0.02 0.008 0.012 0.003 0.003 99.895 7.769 0 0.347 0.04 0.144 0.8 0.023 3.878 1.92 0.089 0.004 0.004 0.003 15.012 Metamorphic T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph6p1 53.02 0 3.07 0.154 11.72 0.141 16.05 12.87 0.416 0.026 0.003 0.013 0.001 0.003 99.494 7.589 0 0.518 0.017 0.282 1.121 0.017 3.425 1.974 0.116 0.005 0.001 0.003 15.063 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph6p2 56.06 0 1.672 0.007 10.43 0.175 17.02 13.06 0.178 0 0.019 0 0.008 0 100.725 7.892 0 0.277 0.001 0 1.228 0.021 3.572 1.97 0.048 0 0.009 0 15.01 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph6p3 55.81 0.063 1.33 0.031 9.8 0.119 17.56 13.14 0.157 0.011 0.047 0.011 0.02 0.002 100.165 7.884 0.007 0.221 0.003 0.001 1.157 0.014 3.698 1.989 0.043 0.002 0.021 0.003 15.019 Si-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph7p1 47.81 0.008 7.46 0.144 15.58 0.294 13.03 11.82 1.39 0.224 0.005 0 0.002 0 99.872 6.897 0.001 1.268 0.016 1.034 0.846 0.036 2.802 1.827 0.389 0.041 0.002 0 15.158 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph7p2 47.06 0.008 8.14 0.159 15.3 0.268 12.93 11.68 1.41 0.257 0.053 0.013 0.022 0.003 99.366 6.857 0.001 1.398 0.018 0.815 1.049 0.033 2.809 1.823 0.398 0.048 0.024 0.003 15.25 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph7p3 49.12 0.023 6.85 0.124 14.21 0.3 13.5 11.54 1.246 0.169 0 0.027 0 0.006 99.19 7.095 0.003 1.166 0.014 0.798 0.919 0.037 2.907 1.786 0.349 0.031 0 0.006 15.104 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph8p1 52.32 0.016 3.95 0.125 14.06 0.153 14.16 12.29 0.577 0.008 0.021 0.001 0.009 0 99.784 7.535 0.002 0.67 0.014 0.34 1.353 0.019 3.04 1.896 0.161 0.002 0.01 0 15.032 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph8p2 51.53 0.085 4.57 0.227 13.38 0.189 14.03 11.98 0.7 0.029 0.086 0.006 0.036 0.001 98.881 7.475 0.009 0.781 0.026 0.351 1.272 0.023 3.034 1.862 0.197 0.005 0.039 0.002 15.037 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph8p3 51.84 0.016 4.44 0.085 14.02 0.156 14.13 12.13 0.678 0.002 0.053 0.001 0.022 0 99.602 7.466 0.002 0.754 0.01 0.425 1.263 0.019 3.034 1.872 0.189 0 0.024 0 15.033 Al-amphibole T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph9p1 55.06 0.004 2.2 0.329 9.98 0.263 17.1 12.23 0.465 0.017 0 0.001 0 0 99.76 7.782 0 0.366 0.037 0.197 0.982 0.031 3.603 1.852 0.127 0.003 0 0 14.982 Metamorphic T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph9p2 55.07 0 2.5 0.267 9.44 0.219 17.28 12.54 0.5 0.022 0.038 0.004 0.016 0.001 99.98 7.776 0 0.416 0.03 0.068 1.047 0.026 3.637 1.897 0.137 0.004 0.017 0.001 15.038 Metamorphic T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_088Amph9p3 54.05 0.051 3.51 0.423 8.98 0.204 17.46 12.56 0.502 0.043 0 0.005 0 0.001 99.886 7.615 0.005 0.583 0.047 0.192 0.866 0.024 3.667 1.896 0.137 0.008 0 0.001 15.041 Metamorphic T.S. block MCD0362 910.9 2331.77 0.0181 2.197674419M400_089Amph1p1 50.3 0.624 5.27 0 15.76 0.294 12.6 11.79 0.816 0.057 0.022 0.018 0.009 0.004 99.654 7.314 0.068 0.903 0 0.48 1.436 0.036 2.731 1.837 0.23 0.011 0.01 0.004 15.047 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph1p2 50.75 0.386 5.25 0 15.39 0.308 12.98 11.71 0.858 0.06 0 0.016 0 0.004 99.807 7.34 0.042 0.895 0 0.512 1.35 0.038 2.799 1.815 0.241 0.011 0 0.004 15.041 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph1p3 52.53 0.195 3.16 0 15.1 0.329 13.85 12.21 0.507 0.06 0 0.049 0 0.011 100.091 7.583 0.021 0.538 0 0.352 1.471 0.04 2.981 1.889 0.142 0.011 0 0.012 15.027 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph2p1 50.04 0.093 5.61 0 19.15 0.184 10.67 10.86 0.94 0.024 0.005 0.005 0.002 0.001 99.678 7.326 0.01 0.968 0 0.682 1.663 0.023 2.329 1.703 0.267 0.004 0.002 0.001 14.975 Metamorphic T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph2p2 48.55 0.043 6.72 0 21 0.259 9.72 10.86 1.033 0.035 0.036 0.027 0.015 0.006 100.375 7.253 0.005 1.183 0 0 2.624 0.033 2.165 1.738 0.299 0.007 0.017 0.007 15.306 Metamorphic T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph2p3 50.57 0.169 5.25 0 17.88 0.171 11.96 11.04 0.872 0.042 0 0.018 0 0.004 100.059 7.463 0.019 0.913 0 0 2.207 0.021 2.631 1.746 0.249 0.008 0 0.004 15.257 Metamorphic T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph3p1 50.53 0.061 5.32 0 15.53 0.343 12.82 10.59 1.255 0.025 0 0.018 0 0.004 98.593 7.359 0.007 0.913 0 0.697 1.195 0.042 2.784 1.653 0.354 0.005 0 0.004 15.008 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph3p2 51.68 0.174 4.2 0 13.73 0.279 14.52 11.72 0.756 0.063 0 0.042 0 0.009 99.267 7.449 0.019 0.713 0 0.528 1.127 0.034 3.12 1.81 0.211 0.012 0 0.01 15.023 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph3p3 50.78 0.051 5 0 14.01 0.324 14.19 11.51 1.051 0.092 0 0.084 0 0.019 99.179 7.327 0.005 0.85 0 0.682 1.009 0.04 3.052 1.779 0.294 0.017 0 0.02 15.056 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph4p1 49.98 0.256 6.33 0.003 14.48 0.524 13.61 10.6 1.27 0.106 0 0 0 0 99.246 7.185 0.028 1.072 0 0.851 0.889 0.064 2.917 1.633 0.354 0.019 0 0 15.012 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph4p2 51.75 0 3.95 0 11.57 0.293 15.86 12.13 0.557 0.069 0 0 0 0 98.248 7.5 0 0.675 0 0.313 1.09 0.036 3.426 1.883 0.157 0.013 0 0 15.091 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_089Amph4p3 51.66 0.131 4.57 0 13.43 0.276 14.52 11.77 0.801 0.077 0.03 0.005 0.013 0.001 99.323 7.431 0.014 0.775 0 0.504 1.111 0.034 3.114 1.814 0.223 0.014 0.014 0.001 15.034 Si-amphibole T.S. block MCD0362 1067 2340.44 NULL 6.329787234M400_098Amph1p1 51.78 0.334 5.65 0.166 13.27 0.173 14.43 11.49 0.886 0.119 0 0.024 0 0.005 100.419 7.353 0.036 0.946 0.019 0.49 1.086 0.021 3.055 1.748 0.244 0.022 0 0.006 15.017 Si-amphibole T.S. block MCD0393 193.7 2336.83 NULL 2.156593407M400_098Amph1p2 52.01 0.418 5.26 0.094 13.31 0.168 14.48 11.45 0.512 0.102 0.073 0.028 0.031 0.006 99.98 7.486 0.045 0.892 0.011 0.016 1.586 0.021 3.107 1.766 0.143 0.019 0.033 0.007 15.091 Si-amphibole T.S. block MCD0393 193.7 2336.83 NULL 2.156593407M400_098Amph1p3 51.99 0.501 5.5 0.069 13.34 0.168 14.57 11.23 0.671 0.103 0.073 0.024 0.031 0.005 100.277 7.381 0.054 0.92 0.008 0.484 1.1 0.02 3.084 1.708 0.185 0.019 0.033 0.006 14.961 Si-amphibole T.S. block MCD0393 193.7 2336.83 NULL 2.156593407M400_102Amph1p1 55.02 0.007 0.856 0.02 14.93 1.253 13.97 12.43 0.11 0.014 0.025 0.013 0.011 0.003 100.712 7.925 0.001 0.145 0.002 0.084 1.714 0.153 3 1.918 0.031 0.003 0.012 0.003 14.975 Si-amphibole T.S. block MCD0393 352.3 2339.82 NULL 3.045045045M400_102Amph1p2 55.59 0.014 0.572 0.001 15.26 1.192 13.47 12.61 0.052 0.007 0 0 0 0 100.846 8.028 0.002 0.097 0 0 1.843 0.146 2.9 1.951 0.015 0.001 0 0 14.983 Si-amphibole T.S. block MCD0393 352.3 2339.82 NULL 3.045045045M400_102Amph1p3 55.63 0.036 0.909 0 13.91 1.079 14.22 12.62 0.087 0.038 0 0.003 0 0.001 100.608 8.002 0.004 0.154 0 0 1.673 0.132 3.049 1.945 0.024 0.007 0 0.001 14.991 Si-amphibole T.S. block MCD0393 352.3 2339.82 NULL 3.045045045M400_106Amph1p1 50.97 0.051 4.9 0 20.42 0.319 9.93 11.92 0.523 0.06 0 0.029 0 0.007 101.227 7.451 0.006 0.844 0 0.35 2.146 0.039 2.164 1.867 0.148 0.011 0 0.007 15.026 Metamorphic T.S. block MCD0428 358.5 2335.14 0.0505 12.08M400_106Amph1p2 51.51 0.067 4.45 0.008 19.81 0.349 10.27 11.94 0.467 0.061 0.016 0 0.007 0 101.05 7.525 0.007 0.766 0.001 0.286 2.134 0.043 2.237 1.869 0.132 0.011 0.007 0 15.013 Metamorphic T.S. block MCD0428 358.5 2335.14 0.0505 12.08M400_106Amph1p3 50.51 0.063 4.89 0.026 20.24 0.354 10.08 11.9 0.562 0.065 0 0.006 0 0.001 100.805 7.476 0.007 0.853 0.003 0.004 2.501 0.044 2.224 1.887 0.161 0.012 0 0.001 15.174 Metamorphic T.S. block MCD0428 358.5 2335.14 0.0505 12.08M400_106Amph2p1 54.04 0 1.499 0.03 16.62 0.289 12.48 12.64 0.134 0.031 0 0.01 0 0.002 99.888 7.924 0 0.259 0.004 0 2.038 0.036 2.728 1.986 0.038 0.006 0 0.002 15.019 Si-amphibole T.S. block MCD0428 358.5 2335.14 0.0505 12.08M400_106Amph2p2 54.55 0.004 2.26 0.038 15.68 0.307 13.61 12.38 0.171 0.038 0.038 0.017 0.016 0.004 101.188 7.815 0 0.382 0.004 0.079 1.8 0.037 2.907 1.9 0.047 0.007 0.017 0.004 14.979 Si-amphibole T.S. block MCD0428 358.5 2335.14 0.0505 12.08M400_106Amph2p3 52.97 0.043 3.85 0.002 15.01 0.215 13.61 12.82 0.334 0.117 0.03 0.001 0.013 0 101.084 7.587 0.005 0.65 0 0.173 1.625 0.026 2.906 1.967 0.093 0.021 0.014 0 15.054 Si-amphibole T.S. block MCD0428 358.5 2335.14 0.0505 12.08M400_109Amph1p1 52.91 0.026 1.633 0 24.8 0.559 7.9 11.76 0.192 0.033 0.008 0 0.003 0 101.921 7.851 0.003 0.286 0 0.136 2.942 0.07 1.748 1.87 0.055 0.006 0.004 0 14.966 Si-amphibole T.S. block MCD0428 440.55 2339.52 NULL 9.15601023M400_109Amph1p2 51.76 0.045 2.46 0.012 24.52 0.485 7.99 12.05 0.353 0.043 0 0.012 0 0.003 101.84 7.683 0.005 0.43 0.001 0.267 2.776 0.061 1.768 1.916 0.101 0.008 0 0.003 15.018 Si-amphibole T.S. block MCD0428 440.55 2339.52 NULL 9.15601023M400_109Amph1p3 52.66 0.019 1.521 0.008 24.98 0.571 7.92 12.02 0.208 0.04 0 0.003 0 0.001 102.063 7.841 0.002 0.267 0.001 0.037 3.073 0.072 1.758 1.918 0.06 0.008 0 0.001 15.038 Si-amphibole T.S. block MCD0428 440.55 2339.52 NULL 9.15601023
A-5
M400_109Amph2p1 43.83 0.019 10.22 0 26.62 0.394 4.69 11.61 1.145 0.176 0 0.025 0 0.006 100.781 6.64 0.002 1.825 0 0.853 2.519 0.051 1.059 1.884 0.336 0.034 0 0.006 15.204 Al-amphibole T.S. block MCD0428 440.55 2339.52 NULL 9.15601023M400_109Amph2p2 45.07 0.015 8.89 0 26.45 0.419 5.14 11.62 1.136 0.173 0 0.027 0 0.006 101.044 6.813 0.002 1.584 0 0.75 2.593 0.054 1.158 1.882 0.333 0.033 0 0.007 15.202 Al-amphibole T.S. block MCD0428 440.55 2339.52 NULL 9.15601023M400_109Amph2p3 44.7 0.019 9.53 0.008 26.86 0.38 4.97 11.58 1.079 0.204 0.04 0.027 0.017 0.006 101.484 6.733 0.002 1.692 0.001 0.795 2.588 0.048 1.116 1.869 0.315 0.039 0.019 0.007 15.198 Al-amphibole T.S. block MCD0428 440.55 2339.52 NULL 9.15601023M400_115Amph1p1 55.94 0.048 1.123 0.05 9.78 0.247 17.12 12.71 0.128 0 0.065 0 0.027 0 99.299 7.97 0.005 0.189 0.006 0 1.165 0.03 3.636 1.94 0.035 0 0.029 0 14.975 Metamorphic T.S. block CD10628 444.31 2337.52 NULL 1.648648649M400_115Amph1p2 56.18 0.015 0.811 0.02 9.28 0.2 17.59 12.79 0.057 0.012 0 0.002 0 0 99.043 7.998 0.002 0.136 0.002 0 1.105 0.024 3.733 1.951 0.016 0.002 0 0 14.969 Metamorphic T.S. block CD10628 444.31 2337.52 NULL 1.648648649M400_115Amph1p3 53.25 0.095 3.59 0.029 11.41 0.236 15.61 12.35 0.353 0.052 0.056 0.01 0.024 0.002 99.132 7.642 0.01 0.607 0.003 0.18 1.189 0.029 3.339 1.899 0.098 0.009 0.026 0.002 15.007 Metamorphic T.S. block CD10628 444.31 2337.52 NULL 1.648648649M400_115Amph2p1 45.16 0.337 11.63 0.139 15.79 0.265 10.17 11.97 1.159 0.25 0.03 0.005 0.013 0.001 98.982 6.634 0.037 2.014 0.016 0.679 1.26 0.033 2.227 1.884 0.33 0.047 0.014 0.001 15.163 Al-amphibole T.S. block CD10628 444.31 2337.52 NULL 1.648648649M400_115Amph2p2 44.32 0.318 12.61 0.112 16.73 0.263 9.84 11.86 1.179 0.278 0 0.003 0 0.001 99.614 6.474 0.035 2.171 0.013 0.875 1.169 0.033 2.143 1.856 0.334 0.052 0 0.001 15.154 Al-amphibole T.S. block CD10628 444.31 2337.52 NULL 1.648648649M400_115Amph2p3 45.89 0.228 10.88 0.085 15.71 0.262 10.94 12.03 1.083 0.225 0 0.023 0 0.005 99.468 6.688 0.025 1.869 0.01 0.761 1.153 0.032 2.377 1.878 0.306 0.042 0 0.006 15.141 Al-amphibole T.S. block CD10628 444.31 2337.52 NULL 1.648648649M400_116Amph1p1 54.75 0.121 3.63 0 8.26 0.216 18.11 12.68 0.368 0.038 0.082 0.003 0.035 0.001 100.31 7.636 0.013 0.597 0 0.209 0.754 0.025 3.765 1.895 0.1 0.007 0.036 0.001 15.001 Metamorphic T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph1p2 54.71 0.06 3.65 0 8.33 0.214 17.7 12.78 0.376 0.068 0.003 0 0.001 0 99.968 7.681 0.006 0.604 0 0.061 0.917 0.025 3.705 1.922 0.102 0.012 0.001 0 15.037 Metamorphic T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph1p3 54.01 0.075 4.37 0.024 8.83 0.212 17.27 12.67 0.452 0.066 0 0.005 0 0.001 100.099 7.587 0.008 0.723 0.003 0.136 0.902 0.025 3.617 1.907 0.123 0.012 0 0.001 15.042 Metamorphic T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph2p1 48.77 0.179 9.25 0.006 12.25 0.203 13.94 12.08 1.104 0.144 0.062 0 0.026 0 100.074 6.931 0.019 1.549 0.001 0.673 0.783 0.024 2.953 1.839 0.304 0.026 0.028 0 15.103 Al-amphibole T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph2p2 48.9 0.231 9.14 0.027 12.1 0.257 14.12 12.22 1.126 0.158 0 0 0 0 100.396 6.926 0.025 1.526 0.003 0.675 0.759 0.031 2.981 1.854 0.309 0.029 0 0 15.117 Al-amphibole T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph2p3 49.62 0.418 8.37 0.022 11.77 0.242 14.64 12.15 0.915 0.115 0.054 0.023 0.023 0.005 100.429 7.013 0.044 1.394 0.002 0.622 0.769 0.029 3.084 1.84 0.251 0.021 0.024 0.006 15.069 Al-amphibole T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph3p1 58.2 0 0.546 0.007 7.23 0.159 19.38 13.22 0.046 0.032 0.093 0 0.039 0 100.99 8 0 0.089 0.001 0 0.831 0.018 3.971 1.947 0.012 0.006 0.041 0 14.875 Metamorphic T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph3p2 57.93 0.049 0.62 0 7.59 0.135 19.21 13.13 0.047 0.034 0.056 0 0.024 0 100.853 8 0.005 0.101 0 0 0.877 0.016 3.955 1.943 0.013 0.006 0.024 0 14.914 Metamorphic T.S. block CD10628 460.0854 2314.03 0.0154M400_116Amph3p3 57.82 0.015 0.667 0 7.81 0.155 19.15 13.2 0.106 0.04 0.053 0.007 0.022 0.002 101.091 8 0.002 0.109 0 0 0.904 0.018 3.95 1.957 0.028 0.007 0.023 0.002 14.974 Metamorphic T.S. block CD10628 460.0854 2314.03 0.0154M400_124Amph1pt1 55.85 0.058 0.421 0.015 13.88 0.416 15.14 12.1 0.084 0.043 0.111 0.005 0.047 0.001 100.192 8.018 0.006 0.071 0.002 0.018 1.648 0.051 3.24 1.861 0.023 0.008 0.05 0.001 14.946 Si-amphibole T.S. block TD10229 184.5 2314.02 0.0905M400_124Amph1pt2 56.1 0 0.449 0.003 14.41 0.42 15.09 12.24 0.088 0.041 0.136 0.015 0.057 0.003 100.995 7.998 0 0.075 0 0.059 1.659 0.051 3.207 1.87 0.024 0.007 0.061 0.004 14.951 Si-amphibole T.S. block TD10229 184.5 2314.02 0.0905M400_124Amph1pt3 56.29 0 0.32 0.013 14.19 0.432 15.26 12.25 0.061 0.021 0 0.018 0 0.004 100.901 8.016 0 0.054 0.001 0.047 1.643 0.052 3.24 1.869 0.017 0.004 0 0.004 14.943 Si-amphibole T.S. block TD10229 184.5 2314.02 0.0905M400_124Amph2pt1 55.7 0 0.307 0 15.42 0.41 13.78 12.97 0.048 0.023 0.086 0.009 0.036 0.002 100.826 8.05 0 0.052 0 0 1.864 0.05 2.969 2.008 0.013 0.004 0.039 0.002 15.011 Si-amphibole T.S. block TD10229 184.5 2314.02 0.0905M400_124Amph2pt2 55.65 0 0.255 0 15.53 0.435 13.84 12.99 0.015 0.005 0.005 0.006 0.002 0.001 100.8 8.036 0 0.043 0 0 1.876 0.053 2.98 2.01 0.004 0.001 0.002 0.001 15.003 Si-amphibole T.S. block TD10229 184.5 2314.02 0.0905M400_124Amph2pt3 55.8 0.015 0.231 0 15.19 0.381 13.79 12.97 0.06 0.006 0.128 0 0.054 0 100.631 8.077 0.002 0.039 0 0 1.839 0.047 2.976 2.012 0.017 0.001 0.059 0 15.009 Si-amphibole T.S. block TD10229 184.5 2314.02 0.0905M400_128Amph1p1 54.79 0.097 2.91 0 10.8 0.264 16.45 12.11 0.461 0.035 0.039 0.017 0.016 0.004 100.008 7.747 0.01 0.485 0 0.163 1.114 0.032 3.467 1.835 0.126 0.006 0.017 0.004 14.985 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph1p2 55.98 0.064 2.02 0.023 9.84 0.25 17.37 12.33 0.354 0.031 0.021 0.02 0.009 0.004 100.384 7.859 0.007 0.334 0.003 0.075 1.08 0.03 3.635 1.855 0.096 0.005 0.009 0.005 14.979 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph1p3 55.51 0.049 2.49 0.023 11.07 0.239 16.69 12.27 0.45 0.037 0 0.001 0 0 100.931 7.782 0.005 0.411 0.003 0.164 1.134 0.028 3.488 1.843 0.122 0.007 0 0 14.988 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph2p1 54.49 0.082 3.09 0.033 12.23 0.391 15.27 11.72 0.724 0.041 0 0.002 0 0 100.189 7.743 0.009 0.517 0.004 0.185 1.268 0.047 3.235 1.784 0.199 0.007 0 0 14.999 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph2p2 55.2 0.101 2.5 0.017 12.28 0.355 15.96 11.54 0.714 0.024 0 0.007 0 0.002 100.812 7.768 0.011 0.415 0.002 0.287 1.158 0.042 3.348 1.74 0.195 0.004 0 0.002 14.969 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph2p3 55.18 0.052 2.64 0 11.67 0.31 16.21 11.83 0.623 0.025 0 0.005 0 0.001 100.659 7.766 0.006 0.438 0 0.233 1.14 0.037 3.401 1.784 0.17 0.004 0 0.001 14.98 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph3p1 56.81 0.008 1.201 0.005 8.77 0.234 18.1 12.77 0.197 0.008 0 0 0 0 100.24 7.97 0.001 0.199 0.001 0 1.029 0.028 3.786 1.92 0.054 0.001 0 0 14.987 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph3p2 56.23 0.041 1.778 0 9.03 0.221 17.87 12.75 0.296 0.029 0 0.007 0 0.002 100.388 7.884 0.004 0.294 0 0.01 1.049 0.026 3.735 1.915 0.08 0.005 0 0.002 15.003 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_128Amph3p3 56.61 0 1.372 0.032 8.24 0.21 18.32 12.99 0.202 0.011 0 0 0 0 100.123 7.943 0 0.227 0.003 0 0.967 0.025 3.832 1.953 0.055 0.002 0 0 15.006 Si-amphibole T.S. block BUGD049 194.88-194.93 2331.78 NULL 2.437262357M400_132Amph1p1 56.32 0.119 1.529 0.112 9.81 0.213 17.33 12.8 0.171 0.03 0.051 0 0.022 0 100.601 7.921 0.013 0.253 0.012 0 1.154 0.025 3.633 1.929 0.047 0.005 0.023 0 14.992 Si-amphibole T.S. block CD5026 197.9 2312.01 0.0552 1.332432432M400_132Amph1p2 56.7 0.042 1.376 0.031 9.42 0.189 17.7 12.93 0.152 0.009 0 0.011 0 0.002 100.65 7.947 0.004 0.227 0.003 0 1.104 0.022 3.699 1.942 0.041 0.002 0 0.003 14.993 Si-amphibole T.S. block CD5026 197.9 2312.01 0.0552 1.332432432M400_132Amph1p3 56.51 0.084 1.453 0.164 9.58 0.203 17.77 12.73 0.177 0.018 0 0 0 0 100.832 7.904 0.009 0.239 0.018 0.009 1.112 0.024 3.705 1.908 0.048 0.003 0 0 14.979 Si-amphibole T.S. block CD5026 197.9 2312.01 0.0552 1.332432432M400_133Amph1p1 56.7 0.041 1.35 0.173 10.57 0.255 16.96 12.89 0.058 0.038 0.024 0 0.01 0 101.162 7.943 0.004 0.223 0.019 0 1.238 0.03 3.542 1.935 0.016 0.007 0.011 0 14.957 Metamorphic T.S. block td10629 161-162 2318.54 0.0434 1.717861206M400_133Amph1p2 56.61 0 1.271 0.092 10.53 0.188 17.1 12.85 0.071 0.023 0 0.003 0 0.001 100.844 7.944 0 0.21 0.01 0.004 1.232 0.022 3.577 1.932 0.019 0.004 0 0.001 14.955 Metamorphic T.S. block td10629 161-162 2318.54 0.0434 1.717861206M400_133Amph1p3 56.38 0 1.305 0.032 11.09 0.196 16.95 12.52 0.105 0.033 0 0.011 0 0.003 100.737 7.911 0 0.216 0.004 0.161 1.141 0.023 3.545 1.882 0.028 0.006 0 0.003 14.917 Metamorphic T.S. block td10629 161-162 2318.54 0.0434 1.717861206M400_133Amph2p1 53.5 0.123 4.04 0.031 11.79 0.273 16 12.05 0.726 0.049 0 0 0 0 100.712 7.533 0.013 0.67 0.003 0.39 0.998 0.033 3.359 1.818 0.198 0.009 0 0 15.025 Metamorphic T.S. block td10465 150-151 2315.06 0.0383 3.035714286M400_133Amph2p2 53.32 0.075 4.31 0.175 11.8 0.208 16.16 12.11 0.721 0.045 0 0.004 0 0.001 101.056 7.475 0.008 0.712 0.019 0.461 0.923 0.025 3.377 1.819 0.196 0.008 0 0.001 15.023 Metamorphic T.S. block td10465 150-151 2315.06 0.0383 3.035714286M400_133Amph2p3 54.58 0.071 3.35 0.24 10.84 0.206 16.67 12.06 0.593 0.04 0.008 0.001 0.003 0 100.772 7.641 0.007 0.553 0.027 0.338 0.931 0.024 3.479 1.809 0.161 0.007 0.003 0 14.977 Metamorphic T.S. block td10465 150-151 2315.06 0.0383 3.035714286M400_133Amph3p1 56.67 0.049 1.158 0.026 8.6 0.193 18.64 12.62 0.221 0 0.106 0 0.044 0 100.381 7.916 0.005 0.191 0.003 0.079 0.926 0.023 3.882 1.889 0.06 0 0.047 0 14.973 Si-amphibole T.S. block td10465 150-151 2315.06 0.0383 3.035714286M400_133Amph3p2 55.88 0.094 2.14 0.133 9.18 0.229 17.63 12.41 0.414 0.036 0.126 0.003 0.053 0.001 100.289 7.84 0.01 0.354 0.015 0.061 1.016 0.027 3.687 1.865 0.113 0.006 0.056 0.001 14.995 Si-amphibole T.S. block td10465 150-151 2315.06 0.0383 3.035714286M400_133Amph3p3 56.09 0.064 2.09 0.187 9.34 0.223 17.61 12.25 0.384 0.02 0.089 0 0.038 0 100.369 7.856 0.007 0.345 0.021 0.07 1.024 0.026 3.677 1.838 0.104 0.004 0.04 0 14.973 Si-amphibole T.S. block td10465 150-151 2315.06 0.0383 3.035714286M400_140Amph1p1 42.95 0.688 11.17 0.016 21.92 0.286 7.13 10.99 1.86 0.117 0.016 0.119 0.007 0.027 99.344 6.504 0.078 1.994 0.002 0.705 2.071 0.037 1.61 1.783 0.546 0.023 0.007 0.031 15.352 Metamorphic T.S. block HRD0026 156.46-156.51 2335.08 NULL 2.587719298M400_140Amph1p3 43.17 0.49 10.23 0 20.14 0.229 8.62 11.32 1.61 0.788 0 0.354 0 0.08 98.947 6.565 0.056 1.834 0 0.608 1.954 0.029 1.954 1.844 0.475 0.153 0 0.091 15.472 Metamorphic T.S. block HRD0026 156.46-156.52 2335.08 NULL 2.587719298M400_140Amph2p1 54.69 0.043 1.2 0.012 19.05 0.24 12.17 12.37 0.212 0.058 0 0.001 0 0 102.121 7.872 0.005 0.204 0.001 0.126 2.167 0.029 2.611 1.908 0.059 0.011 0 0 14.993 Si-amphibole T.S. block HRD0026 156.46-156.53 2335.08 NULL 2.587719298M400_140Amph2p2 55.02 0 0.862 0.004 17.83 0.222 12.54 12.43 0.132 0.037 0 0 0 0 101.146 7.972 0 0.147 0 0 2.16 0.027 2.709 1.93 0.037 0.007 0 0 14.989 Si-amphibole T.S. block HRD0026 156.46-156.54 2335.08 NULL 2.587719298M400_140Amph2p3 54.01 0 1.448 0 18.36 0.226 12.3 12.37 0.248 0.022 0 0.001 0 0 101.052 7.838 0 0.248 0 0.149 2.08 0.028 2.661 1.923 0.07 0.004 0 0 15 Si-amphibole T.S. block HRD0026 156.46-156.55 2335.08 NULL 2.587719298
PTS_017_amph1_pt1 42.15 0.099 14.01 0 20.79 0.255 6.91 11.82 1.44 0.379 0.002 0 0.001 0 99.832 6.259 0.011 2.452 0 1.033 1.549 0.032 1.53 1.88 0.415 0.072 0.001 0 15.231 Al-amphibole HyLogger-1 CD10662 375.59 2326.39 0.015PTS_017_amph1_pt2 41.35 0.175 14.58 0.013 21.73 0.248 6.5 11.73 1.47 0.454 0.048 0.005 0.02 0.001 100.399 6.158 0.02 2.559 0.002 0.992 1.715 0.031 1.443 1.872 0.424 0.086 0.023 0.001 15.301 Al-amphibole HyLogger-1 CD10662 375.59 2326.39 0.015PTS_017_amph1_pt3 41.42 0.046 14.41 0.009 21.72 0.216 6.72 11.48 1.49 0.434 0.012 0 0.005 0 100.044 6.18 0.005 2.534 0.001 1.006 1.704 0.027 1.495 1.835 0.431 0.083 0.006 0 15.301 Al-amphibole HyLogger-1 CD10662 375.59 2326.39 0.015PTS_019_amph1_pt1 44.09 0.115 11.8 0 19.68 0.267 9.06 11.32 1.345 0.264 0.053 0.014 0.022 0.003 100.094 6.504 0.013 2.051 0 0.861 1.567 0.033 1.992 1.789 0.385 0.05 0.024 0.004 15.244 Al-amphibole T.S. block CD10662 376.75 2338.55 NULL 2.316602317PTS_019_amph1_pt2 43.31 0.134 11.95 0.018 20.31 0.251 8.4 11.68 1.338 0.26 0.024 0.004 0.01 0.001 99.756 6.431 0.015 2.091 0.002 0.961 1.561 0.032 1.859 1.858 0.385 0.049 0.011 0.001 15.244 Al-amphibole T.S. block CD10662 376.75 2338.55 NULL 2.316602317PTS_019_amph1_pt3 41.11 0.179 13.91 0.013 21.63 0.263 7.12 11.46 1.52 0.417 0.088 0.016 0.037 0.003 99.788 6.148 0.02 2.452 0.002 1.125 1.58 0.033 1.587 1.836 0.441 0.079 0.042 0.004 15.303 Al-amphibole T.S. block CD10662 376.75 2338.55 NULL 2.316602317PTS_113_amph1_pt1 43.05 0.295 13.46 0.017 16.97 0.341 9.84 11.77 1.332 0.324 0 0.01 0 0.002 99.476 6.319 0.033 2.329 0.002 0.9 1.183 0.042 2.153 1.851 0.379 0.061 0 0.002 15.253 Al-amphibole T.S. block CD10662 827.95 2327.91 0.0259 4.605633803PTS_113_amph1_pt2 43.58 0.129 12.93 0.152 16.37 0.338 10.38 11.78 1.36 0.327 0 0.008 0 0.002 99.467 6.383 0.014 2.232 0.018 0.889 1.116 0.042 2.267 1.849 0.386 0.061 0 0.002 15.257 Al-amphibole T.S. block CD10662 827.95 2327.91 0.0259 4.605633803PTS_113_amph1_pt3 42.58 0.251 13.89 0.163 17.17 0.32 9.74 11.79 1.36 0.342 0 0 0 0 99.652 6.24 0.028 2.399 0.019 0.977 1.127 0.04 2.128 1.851 0.386 0.064 0 0 15.26 Al-amphibole T.S. block CD10662 827.95 2327.91 0.0259 4.605633803PTS_114_amph1_pt1 45.36 0.315 10.21 0.225 14.47 0.22 12.37 11.54 1.68 0.157 0 0 0 0 98.609 6.596 0.034 1.75 0.026 1.113 0.646 0.027 2.682 1.798 0.474 0.029 0 0 15.176 Al-amphibole HyLogger-1 CD10662 925.06 2314.81 0.0319PTS_114_amph1_pt2 45.71 0.178 10.35 0.272 14.65 0.186 12.55 11.52 1.67 0.173 0 0 0 0 99.339 6.591 0.019 1.759 0.031 1.159 0.607 0.023 2.698 1.78 0.467 0.032 0 0 15.165 Al-amphibole HyLogger-1 CD10662 925.06 2314.81 0.0319PTS_114_amph1_pt3 46.06 0.237 9.82 0.39 14.33 0.16 12.56 11.59 1.65 0.137 0 0.004 0 0.001 99.017 6.668 0.026 1.676 0.045 1.047 0.688 0.02 2.711 1.798 0.463 0.025 0 0.001 15.166 Al-amphibole HyLogger-1 CD10662 925.06 2314.81 0.0319WB377_5Amph1p1 46.73 0.385 8.29 0.04 17.94 0.33 10.96 11.69 1.055 0.513 0.163 0.028 0.069 0.006 100.07 6.869 0.043 1.436 0.005 0.658 1.547 0.041 2.402 1.841 0.301 0.096 0.076 0.007 15.238 Metamorphic T.S. block WB0801CD 377 2342.88 NULL 2.144WB377_5Amph1p2 43.8 0.102 16.15 0.146 14.35 0.329 6.32 16.01 0.86 0.152 0.12 0.012 0.05 0.003 100.328 6.449 0.011 2.802 0.017 0 1.767 0.041 1.387 2.526 0.245 0.029 0.056 0.003 15.274 Metamorphic T.S. block WB0801CD 377 2342.88 NULL 2.144WB377_5Amph1p3 45.4 0.198 10.22 0.287 18.68 0.321 9.67 11.78 1.42 0.423 0.13 0.041 0.055 0.009 100.561 6.697 0.022 1.777 0.034 0.543 1.761 0.04 2.126 1.862 0.406 0.08 0.06 0.01 15.347 Metamorphic T.S. block WB0801CD 377 2342.88 NULL 2.144WB377_5Amph1p4 45.68 0.191 10.2 0.125 17.32 0.309 9.9 11.88 1.41 0.272 0.115 0.019 0.048 0.004 99.411 6.791 0.021 1.787 0.015 0.332 1.821 0.039 2.194 1.892 0.406 0.052 0.054 0.005 15.35 Metamorphic T.S. block WB0801CD 377 2342.88 NULL 2.144WB470_8Amph1p1 50.7 0.078 3.76 0.012 19.29 0.774 10.76 11.38 0.744 0.109 0.023 0.008 0.01 0.002 99.682 7.487 0.009 0.654 0.001 0.517 1.865 0.097 2.369 1.801 0.213 0.021 0.011 0.002 15.034 Metamorphic T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph1p2 51.17 0.124 4.2 0.02 16.76 0.579 12.33 11.82 0.672 0.134 0.106 0.003 0.045 0.001 99.977 7.464 0.014 0.722 0.002 0.41 1.635 0.072 2.681 1.847 0.19 0.025 0.049 0.001 15.062 Metamorphic T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph1p3 50.35 0.146 4.73 0.019 17.25 0.536 11.87 11.64 0.8 0.105 0 0.009 0 0.002 99.519 7.386 0.016 0.818 0.002 0.471 1.645 0.067 2.596 1.829 0.228 0.02 0 0.002 15.077 Metamorphic T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph2p1 51.8 0.101 3.72 0.006 16.33 0.544 13.08 11.74 0.64 0.142 0.021 0 0.009 0 100.231 7.583 0.011 0.642 0.001 0 1.999 0.067 2.855 1.841 0.182 0.026 0.01 0 15.208 Metamorphic T.S. block WB0801CD 470 2336.89 0.0196 4.155124654
A-6
WB470_8Amph2p2 51.09 0.079 4.42 0 16.3 0.574 12.64 11.66 0.707 0.1 0.062 0.014 0.026 0.003 99.724 7.436 0.009 0.758 0 0.498 1.486 0.071 2.743 1.818 0.2 0.019 0.029 0.003 15.036 Metamorphic T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph2p3 50.31 0.071 4.67 0.006 17.44 0.702 11.54 11.54 0.761 0.13 0 0.006 0 0.001 99.258 7.411 0.008 0.811 0.001 0.467 1.681 0.088 2.534 1.821 0.217 0.024 0 0.002 15.063 Metamorphic T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph3p1 53.94 0 1.512 0.004 13.53 0.655 14.72 12.92 0.204 0.062 0 0 0 0 99.617 7.811 0 0.258 0 0.107 1.532 0.08 3.178 2.005 0.057 0.011 0 0 15.04 Si-amphibole T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph3p2 54.25 0 1.168 0 12.83 0.616 14.85 13.55 0.172 0.058 0.029 0.01 0.012 0.002 99.589 7.847 0 0.199 0 0.096 1.456 0.075 3.202 2.1 0.048 0.011 0.013 0.002 15.035 Si-amphibole T.S. block WB0801CD 470 2336.89 0.0196 4.155124654WB470_8Amph3p3 55.41 0.015 1.313 0 11.67 0.61 15.69 12.69 0.18 0.041 0 0.006 0 0.001 99.726 7.947 0.002 0.222 0 0 1.4 0.074 3.355 1.95 0.05 0.008 0 0.001 15.008 Si-amphibole T.S. block WB0801CD 470 2336.89 0.0196 4.155124654
PTS_122_amph1_pt1 56.41 0.06 1.289 0.027 5.66 0.275 20.88 12.86 0.238 0.013 0.179 0.004 0.075 0.001 99.937 7.828 0.006 0.211 0.003 0.116 0.541 0.032 4.319 1.912 0.064 0.002 0.078 0.001 15.034 Si-amphibolePTS_122_amph1_pt2 55.35 0.049 1.786 0.028 6.4 0.258 20.4 12.81 0.297 0.019 0.143 0.006 0.06 0.001 99.517 7.723 0.005 0.294 0.003 0.244 0.503 0.031 4.243 1.915 0.08 0.003 0.063 0.001 15.044 Si-amphibolePTS_122_amph1_pt3 55.88 0.079 1.562 0.027 5.82 0.325 20.9 13.07 0.268 0.031 0.218 0 0.092 0 100.136 7.735 0.008 0.255 0.003 0.25 0.424 0.038 4.313 1.938 0.072 0.005 0.095 0 15.042 Si-amphibolePTS_122_amph2_pt1 46.18 0.229 9.86 0.404 13.17 0.239 13.73 12.25 1.322 0.231 0.115 0 0.049 0 99.799 6.719 0.025 1.691 0.046 0.36 1.243 0.029 2.978 1.909 0.373 0.043 0.053 0 15.416 MetamorphicPTS_122_amph2_pt2 47.22 0.118 8.98 0.419 12.42 0.254 14.19 12.29 1.302 0.181 0 0 0 0 99.448 6.822 0.013 1.529 0.048 0.55 0.951 0.031 3.056 1.902 0.365 0.033 0 0 15.3 MetamorphicPTS_122_amph2_pt3 45.76 0.155 10.12 0.478 12.95 0.237 13.59 12.07 1.48 0.271 0.06 0 0.025 0 99.22 6.649 0.017 1.733 0.055 0.655 0.918 0.029 2.944 1.879 0.417 0.05 0.027 0 15.346 MetamorphicPTS_122_amph3_pt1 53.99 0.071 2.88 0.24 7.68 0.196 19.21 12.69 0.394 0.066 0.012 0 0.005 0 99.513 7.608 0.008 0.478 0.027 0.145 0.76 0.023 4.035 1.916 0.108 0.012 0.005 0 15.12 MetamorphicPTS_122_amph3_pt2 53.25 0.034 3.79 0.147 8.23 0.225 18.3 12.63 0.512 0.046 0.143 0 0.06 0 99.358 7.554 0.004 0.634 0.016 0.087 0.89 0.027 3.87 1.92 0.141 0.008 0.064 0 15.149 MetamorphicPTS_122_amph3_pt3 54.53 0.019 2.76 0.154 7.52 0.228 19.12 12.67 0.415 0.048 0.037 0.008 0.016 0.002 99.54 7.682 0.002 0.458 0.017 0.035 0.851 0.027 4.015 1.912 0.113 0.009 0.016 0.002 15.122 MetamorphicPTS_123_amph1_pt1 51.57 0.127 5.42 0.153 10.28 0.232 17.15 12.22 1 0.082 0.261 0.004 0.11 0.001 100.485 7.323 0.014 0.907 0.017 0.112 1.109 0.028 3.631 1.859 0.275 0.015 0.117 0.001 15.29 MetamorphicPTS_123_amph1_pt2 50.79 0.082 5.87 0.091 10.82 0.189 16.5 12.09 1.071 0.109 0.305 0 0.129 0 99.781 7.283 0.009 0.992 0.01 0.096 1.202 0.023 3.527 1.858 0.298 0.02 0.139 0 15.318 MetamorphicPTS_123_amph1_pt3 50.59 0.104 5.99 0.167 10.75 0.195 16.46 11.84 1.137 0.109 0.385 0 0.162 0 99.536 7.183 0.011 1.002 0.019 0.654 0.622 0.023 3.484 1.801 0.313 0.02 0.173 0 15.134 Metamorphic
WB116Amph1p1 55.02 0 1.488 0.015 13.77 0.791 14.74 12.46 0.427 0.125 0.229 0 0.096 0 101.085 7.858 0 0.25 0.002 0.101 1.544 0.096 3.138 1.907 0.118 0.023 0.103 0 15.036 Si-amphiboleWB116Amph1p2 54.45 0 1.667 0 16.36 0.799 12.8 11.73 0.592 0.182 0.246 0 0.104 0 100.73 7.882 0 0.284 0 0.1 1.88 0.098 2.762 1.819 0.166 0.034 0.113 0 15.026 Si-amphiboleWB116Amph1p3 55.02 0.004 0.992 0 15.38 0.788 13.92 12.05 0.458 0.103 0.212 0.001 0.089 0 100.837 7.91 0 0.168 0 0.136 1.713 0.096 2.983 1.856 0.128 0.019 0.096 0 15.01 Si-amphibole
Numbers of ions on the basis of 23 O
A-7
Epidote-Clinoziosite (M400)Sample Number SiO2 TiO2 Al2O3 Cr2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O totals Si Ti Al Cr Fe3+ Fe2+
Mn Mg Ca Na K totals Fe 3+ /(Fe 3+ +Al)*100 Sample HoleID Depth W1550 D1550M400_001ep1pt1 37.7 0.05 22.23 0.02 13.17 1.32 0.09 0 23.54 0.01 0 98.13 3.019 0.003 2.099 0.001 0.793 0.089 0.006 0 2.02 0.002 0 8.032 27.42047026M400_001ep1pt2 37.84 0.07 22.56 0.01 15.12 0.14 0.31 0.02 22.99 0.02 0 99.07 2.997 0.004 2.107 0.001 0.901 0.009 0.021 0.002 1.951 0.003 0 7.996 29.95345745M400_001ep1pt3 37.55 0.04 22.06 0.01 14.47 0.88 0.15 0 23.55 0.01 0.01 98.73 2.997 0.002 2.076 0.001 0.869 0.059 0.01 0 2.014 0.002 0.001 8.03 29.50764007M400_001ep2pt1 37.77 0.06 22.28 0.01 14.34 0.83 0.06 0 23.67 0 0 99.04 3 0.004 2.087 0.001 0.857 0.055 0.004 0 2.017 0 0 8.024 29.11005435M400_001ep2pt2 38.03 0.02 22.34 0.03 13.9 0.8 0.05 0 23.56 0.01 0 98.74 3.022 0.001 2.093 0.002 0.831 0.053 0.003 0 2.006 0.002 0 8.014 28.41997264M400_001ep2pt3 37.86 0 22.39 0 14.51 0.19 0.06 0 23.37 0 0.01 98.39 3.015 0 2.102 0 0.87 0.013 0.004 0 1.994 0 0.001 7.999 29.27321669M400_002ep1pt1 37.85 0.03 22.71 0 12.91 0.98 0.1 0.01 23.48 0.02 0.01 98.1 3.022 0.002 2.137 0 0.776 0.066 0.007 0.001 2.008 0.003 0.001 8.022 26.63920357M400_002ep1pt2 37.72 0 22.65 0.02 14.28 0.13 0.11 0 23.22 0 0 98.15 3.008 0 2.129 0.001 0.857 0.009 0.007 0 1.986 0 0 7.998 28.70060281M400_002ep1pt3 37.97 0 22.7 0 14.22 0.45 0.09 0.01 23.63 0.01 0 99.07 3.005 0 2.118 0 0.847 0.029 0.006 0.001 2.004 0.002 0 8.013 28.56661046M400_003ep1pt1 37.63 0.05 21.02 0.02 14.48 1.71 0.07 0 23.65 0 0 98.65 3.02 0.003 1.989 0.001 0.874 0.115 0.005 0 2.036 0 0 8.044 30.52741879M400_003ep1pt2 37.5 0 21.13 0 17.06 0.16 0.03 0.02 23.19 0 0 99.11 2.992 0 1.987 0 1.024 0.01 0.002 0.002 1.984 0 0 8.002 34.008635M400_003ep1pt3 37.72 0.05 21.23 0.04 15.64 0.86 0.09 0.02 23.46 0.02 0 99.13 3.008 0.003 1.996 0.003 0.939 0.057 0.006 0.002 2.005 0.003 0 8.022 31.99318569M400_003ep2pt1 37.94 0.06 23.78 0 12.96 0.12 0.06 0.01 23 0 0 97.95 3.011 0.004 2.225 0 0.774 0.008 0.004 0.001 1.958 0 0 7.985 25.80860287M400_003ep2pt2 37.55 0.06 21.14 0.01 14.78 1.51 0.02 0 23.71 0 0 98.8 3.009 0.004 1.997 0.001 0.891 0.101 0.001 0 2.038 0 0 8.043 30.85180055M400_003ep2pt3 37.36 0 20.16 0 17.35 0.52 0.02 0 23.36 0.01 0.01 98.79 3.004 0 1.911 0 1.05 0.035 0.001 0 2.013 0.002 0.001 8.017 35.46099291M400_003ep2pt4 37.19 0.07 19.03 0 17.89 1.11 0 0 23.25 0.03 0 98.57 3.015 0.004 1.819 0 1.091 0.075 0 0 2.019 0.005 0 8.028 37.49140893M400_005czo1pt1 38.64 0.12 28.3 0.15 2.85 3.16 0.06 0 24.63 0 0 97.94 3.018 0.007 2.606 0.009 0.168 0.207 0.004 0 2.064 0 0 8.083 6.056236482 T.S. Block BUDG049 33m 1554.26 0.00407M400_005czo1pt2 38.89 0.04 29.05 0.08 3.43 1.83 0.04 0.03 24.4 0 0.01 97.8 3.02 0.002 2.66 0.005 0.201 0.119 0.003 0.003 2.031 0 0.001 8.045 7.025515554 T.S. Block BUDG049 33m 1554.26 0.00407M400_005czo1pt3 39.07 0 29.88 0.09 4.61 0.19 0.05 0.04 24.05 0.01 0.01 97.99 3.009 0 2.713 0.005 0.267 0.012 0.003 0.005 1.984 0.001 0.001 8 8.959731544 T.S. Block BUDG049 33m 1554.26 0.00407M400_005ep1pt1 38.86 0.07 29.35 0 4.64 1.28 0.04 0.01 24.69 0 0.02 98.97 2.988 0.004 2.661 0 0.269 0.082 0.003 0.001 2.034 0 0.002 8.044 9.180887372 T.S. Block BUDG049 33m 1554.26 0.00407M400_005ep1pt2 38.75 0.02 28.24 0.02 6.19 1.13 0.07 0.02 24.49 0 0.01 98.94 2.994 0.001 2.573 0.001 0.36 0.073 0.005 0.002 2.028 0 0.001 8.038 12.27412206 T.S. Block BUDG049 33m 1554.26 0.00407M400_005ep1p3 39.1 0.06 28.5 0.01 7.11 0.06 0.1 0.03 24.01 0 0 99.01 3.005 0.003 2.582 0.001 0.411 0.004 0.007 0.003 1.979 0 0 7.995 13.73204143 T.S. Block BUDG049 33m 1554.26 0.00407M400_005ep2pt1 37.9 0.06 24.04 0 12.33 0.4 0.07 0 23.63 0 0 98.46 2.997 0.004 2.241 0 0.734 0.027 0.005 0 2.004 0 0 8.012 24.67226891 T.S. Block BUDG049 33m 1554.26 0.00407M400_005ep2pt2 37.83 0.05 23.84 0 12.28 0.73 0.05 0.01 23.76 0.01 0 98.56 2.995 0.003 2.225 0 0.731 0.049 0.003 0.001 2.016 0.002 0 8.025 24.72936401 T.S. Block BUDG049 33m 1554.26 0.00407M400_005ep2pt3 37.92 0.06 23.89 0 12.42 0.41 0.09 0.02 23.53 0 0.01 98.35 3.002 0.004 2.23 0 0.74 0.027 0.006 0.002 1.996 0 0.001 8.009 24.91582492 T.S. Block BUDG049 33m 1554.26 0.00407M400_007czo1pt1 38.75 0.09 28.7 0.09 4.93 1.33 0.08 0.02 24.23 0.03 0 98.24 3.004 0.005 2.623 0.006 0.287 0.086 0.005 0.002 2.013 0.005 0 8.035 9.862542955M400_007czo1pt2 38.28 0.06 28.15 0.09 3.7 2.63 0.05 0.39 24.02 0 0 97.39 3.004 0.004 2.604 0.006 0.218 0.173 0.003 0.046 2.022 0 0 8.079 7.725017718M400_007czo1pt3 38.08 0 28.24 0.1 3.92 2.26 0.11 0.03 24.36 0 0.01 97.11 2.998 0 2.621 0.006 0.232 0.149 0.007 0.004 2.055 0 0.001 8.073 8.131791097M400_007czo1pt4 38.62 0.08 28.16 0.08 6.41 0.54 0.04 0.03 23.87 0.02 0 97.85 3.006 0.005 2.584 0.005 0.375 0.035 0.003 0.003 1.991 0.003 0 8.009 12.67320041M400_020ep1pt1 36.01 0.05 24.3 0.03 2.44 7.01 0.11 0.81 24 0.01 0 94.77 2.986 0.003 2.375 0.002 0.153 0.486 0.008 0.1 2.132 0.002 0 8.247 6.05221519M400_022czo1pt1 38.95 0.03 29.54 0 4.77 0.68 0.13 0.02 24.35 0 0 98.5 2.998 0.002 2.681 0 0.277 0.044 0.008 0.002 2.01 0 0 8.022 9.364435429 T.S. Block UDD1420 475.549 1559.02 0.0183M400_022czo1pt2 39.06 0 30.94 0 3 0.31 0.14 0.04 24.22 0 0 97.74 3.002 0 2.803 0 0.174 0.02 0.009 0.005 1.997 0 0 8.009 5.844810212 T.S. Block UDD1420 475.549 1559.02 0.0183M400_022czo1pt3 39.01 0.04 31.04 0.01 3.93 0.04 0.43 0.05 23.45 0 0 98.02 2.991 0.002 2.806 0.001 0.227 0.002 0.028 0.006 1.928 0 0 7.99 7.484338938 T.S. Block UDD1420 475.549 1559.02 0.0183M400_028czo1pt1 38.38 0 28.28 0 3.67 2.34 0.15 0.02 24.47 0 0.01 97.33 3.012 0 2.617 0 0.217 0.154 0.01 0.002 2.058 0 0.001 8.071 7.657021877M400_028czo1pt2 38.7 0 28.41 0 5.98 0.73 0.08 0.02 24.22 0 0 98.16 3.003 0 2.599 0 0.349 0.047 0.005 0.002 2.016 0 0 8.023 11.8385346M400_028czo1pt3 38.66 0 28.49 0 6.59 0.51 0.12 0.02 24.3 0 0 98.71 2.987 0 2.595 0 0.383 0.033 0.008 0.002 2.014 0 0 8.023 12.86098052M400_033czo1pt1 38.42 0.03 27.03 0.36 5.99 2.02 0.07 0.01 23.98 0.01 0 97.92 3.014 0.002 2.5 0.022 0.354 0.133 0.005 0.001 2.016 0.002 0 8.047 12.40364401 T.S. Block UDD1510 239.578 1557.22 0.01925M400_033czo1pt2 38.06 0.04 26.95 0.4 4.79 2.96 0.09 0.03 24.11 0 0 97.45 3.008 0.002 2.511 0.025 0.285 0.196 0.006 0.004 2.044 0 0 8.08 10.19313305 T.S. Block UDD1510 239.578 1557.22 0.01925M400_033czo1pt3 38.39 0.01 26.73 0.39 4.14 3.31 0.08 0.01 24.11 0 0 97.19 3.039 0.001 2.495 0.024 0.246 0.219 0.005 0.001 2.047 0 0 8.078 8.974826706 T.S. Block UDD1510 239.578 1557.22 0.01925M400_033czo2pt1 38.91 0.03 29.44 0.39 0.96 3.08 0.07 0.02 24.36 0 0.01 97.28 3.035 0.002 2.707 0.024 0.057 0.201 0.005 0.002 2.036 0 0.001 8.07 2.062228654 T.S. Block UDD1510 239.578 1557.22 0.01925M400_033czo2pt2 38.85 0.07 29.3 0.37 0.4 3.61 0.11 0.01 24.43 0 0.01 97.16 3.039 0.004 2.702 0.023 0.023 0.236 0.007 0.001 2.047 0 0.001 8.084 0.844036697 T.S. Block UDD1510 239.578 1557.22 0.01925M400_033czo2pt3 38.69 0.09 29.4 0.41 0.69 3.42 0.09 0 24.4 0 0 97.21 3.025 0.005 2.71 0.025 0.041 0.223 0.006 0 2.046 0 0 8.082 1.490367139 T.S. Block UDD1510 239.578 1557.22 0.01925M400_045czo1pt1 38.85 0.02 28.43 0.01 6.64 0.64 0.06 0.07 24.35 0 0 99.1 2.992 0.001 2.581 0.001 0.385 0.042 0.004 0.008 2.011 0 0 8.024 12.98044504M400_045czo1pt2 38.52 0.05 28.94 0 5.87 0.44 0.19 0.03 24.09 0 0 98.16 2.984 0.003 2.643 0 0.343 0.029 0.012 0.003 2.002 0 0 8.02 11.48693905M400_045czo1pt3 38.73 0 29.19 0 6.8 0.06 0.27 0.03 23.96 0 0 99.07 2.974 0 2.643 0 0.393 0.004 0.018 0.003 1.973 0 0 8.008 12.94466403M400_047Czo1p1 39.12 0 30.75 0 0.01 2.34 0.07 0 24.69 0.01 0.01 97 3.035 0 2.813 0 0.001 0.152 0.005 0 2.052 0.002 0.001 8.06 0.035536603M400_047Czo1p2 39.38 0 30.78 0 1.37 1.32 0.11 0.01 24.39 0.01 0 97.38 3.037 0 2.798 0 0.08 0.085 0.007 0.001 2.015 0.001 0 8.025 2.779708131M400_047Czo1p3 39.44 0 30.92 0 1.14 1.37 0.09 0 24.46 0.01 0 97.43 3.038 0 2.808 0 0.066 0.088 0.006 0 2.019 0.001 0 8.026 2.296450939M400_047Czo2p1 39.62 0 32.44 0 0 0.47 0.07 0 24.84 0 0 97.46 3.025 0 2.92 0 0 0.03 0.005 0 2.034 0 0 8.015 0M400_047Czo2p2 39.61 0 32.36 0 0.51 0.6 0.3 0 24.32 0.01 0 97.71 3.022 0 2.91 0 0.029 0.038 0.019 0 1.988 0.001 0 8.009 0.98673018M400_047Czo2p3 39.56 0 32.18 0 0 0.97 0.16 0 24.62 0 0 97.51 3.027 0 2.903 0 0 0.062 0.01 0 2.02 0 0 8.022 0M400_047Czo2p4 39.86 0.03 31.7 0.01 0.76 0.99 0.09 0.02 24.44 0 0.01 97.92 3.041 0.002 2.851 0.001 0.044 0.063 0.006 0.002 1.998 0 0.001 8.009 1.519861831M400_047Czo3p1 38.7 0.09 27.21 0.13 6.52 1.13 0.23 0.02 23.58 0.02 0.03 97.65 3.03 0.005 2.512 0.008 0.384 0.074 0.015 0.002 1.978 0.003 0.003 8.015 13.25966851M400_047Czo3p2 38.58 0.05 27.35 0.13 6.7 0.7 0.18 0.01 23.51 0 0.02 97.23 3.028 0.003 2.53 0.008 0.396 0.046 0.012 0.001 1.977 0 0.002 8.003 13.53383459M400_047Czo3p3 38.79 0.08 27.7 0.01 6.84 0.69 0.22 0.02 23.84 0 0.02 98.21 3.016 0.005 2.539 0.001 0.4 0.045 0.014 0.002 1.986 0 0.002 8.01 13.61007145PTS_017ep1pt1 37.73 0.02 22.68 0 13.91 0.75 0.12 0 23.68 0.02 0.01 98.92 2.996 0.001 2.123 0 0.831 0.05 0.008 0 2.015 0.003 0.001 8.028 28.13134733PTS_017ep1pt2 37.82 0.04 23.47 0.01 12.93 0.5 0.13 0.02 23.53 0 0 98.48 2.999 0.002 2.194 0.001 0.772 0.033 0.009 0.002 2.002 0 0 8.015 26.02832097PTS_017ep1pt3 37.67 0.02 22.58 0.03 13.23 0.98 0.07 0.02 23.53 0 0 98.16 3.01 0.001 2.127 0.002 0.796 0.066 0.005 0.002 2.017 0 0 8.026 27.23229559PTS_019ep1pt1 37.64 0.05 22.55 0.02 13.81 0.37 0.13 0.02 23.15 0 0 97.77 3.014 0.003 2.128 0.001 0.832 0.025 0.009 0.002 1.988 0 0 8.002 28.10810811PTS_019ep1pt2 37.38 0.03 22.26 0.06 13.21 1.27 0.15 0 23.44 0.01 0.01 97.82 3.005 0.002 2.11 0.004 0.799 0.086 0.01 0 2.019 0.002 0.001 8.038 27.46648333PTS_019ep1pt3 37.85 0 24.06 0 11.98 0.41 0.19 0 23.49 0 0 98 3.005 0 2.252 0 0.716 0.027 0.013 0 2 0 0 8.012 24.12398922PTS_019ep2pt1 37.72 0 24.37 0.02 11.07 0.43 0.17 0.01 23.3 0.01 0 97.11 3.012 0 2.294 0.001 0.665 0.029 0.011 0.001 1.993 0.002 0 8.009 22.47380872PTS_019ep2pt2 37.5 0 24.72 0 11.21 0.1 0.17 0.02 23.19 0.04 0 96.95 2.995 0 2.327 0 0.674 0.007 0.012 0.002 1.984 0.006 0 8.008 22.45918027PTS_019ep2pt3 37.16 0 24.25 0 11.69 0.3 0.14 0 23.36 0.03 0 96.93 2.981 0 2.293 0 0.706 0.02 0.01 0 2.008 0.005 0 8.022 23.54118039PTS_113_ep_pt1 37.4 0.04 23.83 0.03 11.93 0.7 0.21 0.02 23.39 0 0.01 97.56 2.99 0.002 2.246 0.002 0.718 0.047 0.014 0.002 2.004 0 0.001 8.026 24.22402159 T.S. Block CD10662 827.95 1547.82 0.0026PTS_113_ep_pt2 37.46 0.06 23.32 0.01 13.49 0.12 0.14 0.01 23.28 0 0 97.91 2.988 0.004 2.193 0.001 0.81 0.008 0.009 0.001 1.992 0 0 8.006 26.97302697 T.S. Block CD10662 827.95 1547.82 0.0026PTS_113_ep_pt3 37.86 0.08 24.12 0 9.45 2.04 0.1 0.01 23.8 0.01 0.01 97.48 3.024 0.005 2.272 0 0.568 0.136 0.007 0.001 2.037 0.002 0.001 8.052 20 T.S. Block CD10662 827.95 1547.82 0.0026M400_054Ep1p1 38.53 0 24.21 0 10.6 1.19 0.11 0.01 23.77 0.01 0.01 98.44 3.04 0 2.252 0 0.629 0.079 0.007 0.001 2.01 0.002 0.001 8.021 21.83269698M400_054Ep1p2 38.08 0 23.87 0 9.01 2.15 0.12 0.01 23.65 0.03 0 96.91 3.055 0 2.258 0 0.544 0.144 0.008 0.001 2.033 0.005 0 8.047 19.41470378M400_054Ep1p3 38.36 0 23.85 0.01 12.33 0.18 0.13 0.03 23.33 0 0.01 98.22 3.032 0 2.223 0.001 0.733 0.012 0.009 0.004 1.976 0 0.001 7.99 24.797023M400_054Ep2p1 38.52 0.01 26.79 0 7.49 1.05 0.05 0.01 24.08 0 0 98.02 3.016 0.001 2.473 0 0.441 0.069 0.003 0.001 2.022 0 0 8.026 15.13383665M400_054Ep3p1 38.94 0 25.37 0.06 9.56 0.87 0.06 0.02 23.81 0.01 0 98.7 3.043 0 2.338 0.004 0.562 0.057 0.004 0.002 1.994 0.002 0 8.005 19.37931034M400_054Ep3p2 39.16 0 25.58 0.12 9.27 1.14 0.13 0.02 23.96 0 0 99.4 3.041 0 2.342 0.007 0.542 0.074 0.009 0.002 1.996 0 0 8.013 18.79334258M400_054Ep3p3 39.16 0.02 24.51 0 11.67 0.56 0.08 0.02 23.91 0 0 99.95 3.039 0.001 2.242 0 0.682 0.036 0.005 0.002 1.99 0 0 7.998 23.32421341
A-8
M400_060Czo1p1 38.52 0.05 24.98 0 10.67 0.1 0.1 0 23.17 0.01 0 97.6 3.041 0.003 2.325 0 0.634 0.006 0.007 0 1.96 0.002 0 7.977 21.42615749M400_060Czo1p2 38.38 0.09 25.04 0.01 9.71 0.62 0.07 0 23.35 0.02 0 97.29 3.041 0.005 2.339 0.001 0.579 0.041 0.005 0 1.982 0.003 0 7.996 19.84235778M400_060Czo1p3 38.33 0.02 25.12 0.01 10.62 0.1 0.15 0 23.34 0 0 97.71 3.026 0.001 2.338 0.001 0.631 0.006 0.01 0 1.976 0 0 7.989 21.25294712M400_060Ep1p1 38.12 0 22.5 0 14.56 0.13 0 0 23.48 0 0 98.81 3.021 0 2.102 0 0.868 0.009 0 0 1.996 0 0 7.995 29.22558923M400_060Ep1p2 38.06 0.01 23.33 0 11.78 0.94 0.15 0.07 23.32 0 0.01 97.67 3.036 0.001 2.194 0 0.707 0.063 0.01 0.008 1.993 0 0.001 8.013 24.37090658M400_060Ep1p3 38.09 0 22.39 0.01 15.1 0.14 0.12 0 23.35 0 0 99.22 3.012 0 2.087 0.001 0.898 0.009 0.008 0 1.98 0 0 7.995 30.08375209M400_061Ep1p1 38.46 0.02 23.36 0.03 13.81 0.13 0.27 0.01 23.18 0 0.01 99.27 3.022 0.001 2.164 0.002 0.817 0.008 0.018 0.001 1.952 0 0.001 7.986 27.40691043M400_061Ep1p2 38.7 0 23.22 0.03 13.64 0.19 0.1 0 23.53 0.02 0.01 99.45 3.035 0 2.147 0.002 0.805 0.013 0.007 0 1.977 0.003 0.001 7.99 27.2696477M400_061Ep1p3 38.58 0.1 22.89 0.01 13.54 0.35 0.23 0.01 23.18 0 0.01 98.9 3.044 0.006 2.129 0.001 0.804 0.023 0.015 0.001 1.96 0 0.001 7.984 27.41220593M400_062Ep1p1 38.18 0 21.82 0.02 15.76 0.14 0.1 0 23.08 0 0 99.12 3.026 0 2.039 0.001 0.94 0.009 0.007 0 1.962 0 0 7.984 31.55421282M400_062Ep1p2 38.21 0.04 22.18 0.01 14.61 0.3 0.12 0.01 23.26 0 0.01 98.74 3.033 0.002 2.075 0.001 0.872 0.02 0.008 0.001 1.978 0 0.001 7.991 29.58941296M400_062Ep1p3 38.23 0.02 22.97 0.01 14.29 0.13 0.25 0 23.04 0 0.01 98.95 3.019 0.001 2.139 0.001 0.849 0.009 0.017 0 1.95 0 0.001 7.986 28.41365462M400_064Ep1p1 39.36 0.04 25.53 0 10.66 0.1 0.13 0 23.68 0.01 0.02 99.53 3.046 0.002 2.329 0 0.621 0.006 0.009 0 1.963 0.002 0.002 7.979 21.05084746M400_066Ep1p1 37.69 0.04 22.12 0 14.32 0.39 0.09 0.04 23.13 0.01 0.01 97.84 3.02 0.002 2.09 0 0.864 0.026 0.006 0.005 1.986 0.002 0.001 8.002 29.24847664M400_066Ep1p2 37.65 0.05 22.18 0.01 13.69 0.5 0.15 0 22.99 0 0.01 97.23 3.031 0.003 2.105 0.001 0.83 0.034 0.01 0 1.983 0 0.001 7.998 28.27938671M400_066Ep1p3 37.81 0 22.45 0.04 12.76 1.19 0.14 0 23.42 0 0.01 97.82 3.03 0 2.121 0.003 0.77 0.079 0.01 0 2.011 0 0.001 8.024 26.63438257M400_071Ep1p1 39.13 0 27.16 0 3.91 2.91 0.1 0.03 24.39 0.03 0 97.66 3.068 0 2.51 0 0.231 0.191 0.007 0.004 2.049 0.005 0 8.064 8.427581175M400_071Ep1p2 39.47 0 27.78 0 4.76 1.95 0.06 0.04 24.4 0 0 98.49 3.058 0 2.537 0 0.278 0.127 0.004 0.005 2.027 0 0 8.035 9.875666075M400_071Ep1p3 39.3 0 26.51 0.01 2.91 3.84 0.15 0.01 24.35 0.02 0 97.1 3.104 0 2.469 0.001 0.173 0.254 0.01 0.001 2.061 0.003 0 8.076 6.548069644M400_071Ep2p1 39.06 0 27.21 0.02 3.58 3.1 0.1 0.01 24.48 0 0 97.59 3.066 0 2.518 0.001 0.212 0.204 0.007 0.001 2.061 0 0 8.069 7.765567766M400_071Ep2p2 39.4 0 28.39 0 6.2 0.47 0.05 0.02 24.15 0 0.01 98.69 3.034 0 2.577 0 0.359 0.03 0.003 0.002 1.992 0 0.001 7.999 12.22752044M400_071Ep2p3 39.16 0.04 28.33 0.03 5.08 1.5 0.07 0.03 24.38 0.01 0 98.63 3.026 0.002 2.581 0.002 0.296 0.097 0.005 0.003 2.019 0.002 0 8.033 10.28849496M400_071Ep3p1 37.98 0 21.79 0 12.05 2.31 0.01 0.01 23.8 0 0.01 97.96 3.052 0 2.064 0 0.728 0.155 0.001 0.001 2.049 0 0.001 8.052 26.07449857M400_071Ep3p2 38.09 0 21.65 0 13.04 1.81 0 0.02 23.7 0 0 98.33 3.049 0 2.043 0 0.785 0.121 0 0.002 2.035 0 0 8.036 27.75813296M400_071Ep3p3 38.23 0.01 22.92 0 10.88 2.16 0.03 0.01 23.91 0 0.01 98.16 3.048 0.001 2.155 0 0.653 0.144 0.002 0.001 2.043 0 0.001 8.048 23.25498575M400_071Ep4p1 38.22 0 26.8 0 0 2.36 0.06 2.64 23.56 0 0.01 93.65 3.081 0 2.547 0 0 0.159 0.004 0.317 2.035 0 0.001 8.145 0M400_071Ep4p2 38.03 0.02 26.32 0 0 2.49 0.03 2.25 23.62 0 0 92.78 3.098 0.001 2.528 0 0 0.17 0.002 0.273 2.064 0 0 8.136 0M400_071Ep4p3 38.34 0 25.67 0 0 2.42 0.01 3.23 23.66 0.02 0 93.35 3.106 0 2.452 0 0 0.164 0.001 0.39 2.054 0.003 0 8.17 0
M400_073Czo1p1 39.85 0.01 29.49 0 1.4 2.3 0.04 0.07 24.37 0.03 0.01 97.57 3.081 0.001 2.688 0 0.081 0.149 0.003 0.008 2.019 0.004 0.001 8.036 2.92524377 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo1p2 39.76 0.09 30.22 0 1.97 1.67 0.1 0.1 24.36 0 0 98.29 3.048 0.005 2.731 0 0.114 0.107 0.006 0.011 2.003 0 0 8.025 4.007029877 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo1p3 39.36 0.04 30.03 0 2.27 1.6 0.22 0.1 24.22 0.03 0 97.87 3.035 0.002 2.73 0 0.132 0.103 0.014 0.011 2.001 0.004 0 8.034 4.612159329 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo2p1 39.78 0.02 30.48 0 1.81 1.45 0.15 0.02 24.45 0 0 98.19 3.048 0.001 2.753 0 0.104 0.093 0.01 0.002 2.009 0 0 8.022 3.640182009 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo2p2 39.63 0.02 30.39 0.01 1.68 1.72 0.14 0 24.57 0.01 0 98.17 3.042 0.001 2.75 0.001 0.097 0.11 0.009 0 2.021 0.001 0 8.033 3.407095188 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo2p3 39.86 0 30.38 0 3.05 0.59 0.13 0 24.23 0.02 0 98.27 3.048 0 2.739 0 0.176 0.038 0.008 0 1.985 0.003 0 7.997 6.037735849 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo3p1 38.99 0 29.53 0.02 4.96 0.05 0.24 0.03 23.46 0.02 0 97.3 3.022 0 2.698 0.001 0.289 0.003 0.016 0.003 1.948 0.003 0 7.985 9.675259458 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo3p2 39.59 0 28.46 0 4.61 1.47 0.06 0.01 24.41 0 0 98.63 3.051 0 2.586 0 0.267 0.094 0.004 0.001 2.018 0 0 8.022 9.358569926 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Czo3p3 39.5 0 29.58 0.02 3.8 0.96 0.24 0.04 24.15 0.01 0 98.3 3.037 0 2.681 0.001 0.22 0.062 0.016 0.005 1.99 0.001 0 8.013 7.583591865 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Ep1p2 38.52 0.02 23.07 0 11.87 1.41 0.01 0.02 23.76 0.03 0.01 98.72 3.048 0.001 2.152 0 0.707 0.093 0.001 0.002 2.014 0.005 0.001 8.024 24.7289262 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Ep1p3 38.74 0.03 23.54 0.03 10.71 1.64 0.04 0.02 23.75 0 0.01 98.5 3.062 0.002 2.193 0.002 0.637 0.108 0.003 0.002 2.011 0 0.001 8.021 22.50883392 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Ep2p1 38.7 0 25.4 0 9.58 0.55 0.18 0 23.56 0 0 97.99 3.042 0 2.354 0 0.567 0.036 0.012 0 1.986 0 0 7.998 19.41116056 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Ep2p2 38.69 0.05 25.28 0 9.31 1.15 0.2 0.02 23.76 0 0 98.48 3.036 0.003 2.339 0 0.549 0.075 0.013 0.002 2 0 0 8.017 19.00969529 T.S. Block LNGT001 172.150 1556.16 0.03455M400_073Ep2p3 38.72 0 24.34 0 11.67 0.36 0.17 0.01 23.56 0.01 0 98.84 3.037 0 2.251 0 0.689 0.023 0.011 0.001 1.98 0.002 0 7.994 23.43537415 T.S. Block LNGT001 172.150 1556.16 0.03455
M400_075Czo1p1 38.44 0.06 23.44 0.03 11.27 0.94 0.06 0.02 23.25 0.01 0 97.53 3.061 0.004 2.2 0.002 0.676 0.063 0.004 0.002 1.984 0.002 0 7.997 23.50486787M400_075Czo1p2 38.61 0.05 23.5 0.02 10.02 1.92 0.09 0.01 23.64 0 0 97.89 3.069 0.003 2.202 0.001 0.599 0.128 0.006 0.001 2.016 0 0 8.026 21.38521956M400_075Czo1p3 38.51 0.06 23.82 0.02 9.7 1.73 0.14 0.01 23.49 0 0 97.51 3.066 0.004 2.236 0.001 0.581 0.115 0.009 0.001 2.006 0 0 8.021 20.62477813M400_075Czo1p4 38.37 0.04 23.91 0.01 9.82 1.74 0.12 0.01 23.65 0 0 97.7 3.053 0.002 2.243 0.001 0.588 0.116 0.008 0.001 2.018 0 0 8.029 20.77004592M400_075Ep1p1 38.38 0 22.32 0.02 13.3 0.54 0.12 0.01 23.08 0 0 97.79 3.064 0 2.101 0.001 0.799 0.036 0.008 0.001 1.976 0 0 7.986 27.55172414M400_075Ep1p2 38.31 0.02 22.17 0.03 11.77 1.79 0.03 0.03 23.41 0 0.01 97.57 3.073 0.001 2.097 0.002 0.711 0.12 0.002 0.004 2.012 0 0.001 8.022 25.32051282M400_075Ep1p3 38.24 0.01 22.64 0 10.52 1.85 0.13 0.02 23.23 0 0.01 96.65 3.084 0.001 2.153 0 0.639 0.125 0.009 0.002 2.007 0 0.001 8.02 22.88681948M400_075Ep2p1 38.17 0.05 22.27 0.03 12.11 1.71 0.09 0.03 23.45 0 0.01 97.92 3.055 0.003 2.101 0.002 0.729 0.115 0.006 0.004 2.011 0 0.001 8.027 25.75971731M400_075Ep2p2 38.73 0 22.4 0.01 12.46 1.3 0.15 0.01 23.44 0.01 0 98.51 3.074 0 2.096 0.001 0.744 0.086 0.01 0.001 1.993 0.002 0 8.007 26.1971831M400_075Ep2p3 38.2 0.02 22.16 0.03 12.85 1.42 0.1 0.02 23.48 0.01 0 98.29 3.049 0.001 2.085 0.002 0.772 0.095 0.007 0.002 2.008 0.002 0 8.022 27.02135107
M400_079Czo1p1 39.38 0.06 25.5 0.02 10.11 0.51 0.24 0 23.7 0.01 0 99.53 3.05 0.003 2.328 0.001 0.589 0.033 0.016 0 1.967 0.002 0 7.989 20.19197806 T.S. Block LNGT001 282.000 1554.87 0.00333M400_079Czo1p2 39.77 0 26.84 0 9.12 0.22 0.23 0 24.05 0 0.01 100.23 3.042 0 2.42 0 0.525 0.014 0.015 0 1.971 0 0.001 7.987 17.82682513 T.S. Block LNGT001 282.000 1554.87 0.00333M400_079Czo1p3 39.56 0 27.32 0 7.62 0.86 0.18 0 24.32 0 0 99.89 3.034 0 2.47 0 0.44 0.055 0.012 0 2 0 0 8.011 15.12027491 T.S. Block LNGT001 282.000 1554.87 0.00333M400_079Czo2p1 39.87 0.02 29.04 0 5.53 0.68 0.18 0.01 24.39 0.01 0 99.73 3.034 0.001 2.605 0 0.317 0.044 0.012 0.001 1.989 0.001 0 8.004 10.84873374 T.S. Block LNGT001 282.000 1554.87 0.00333M400_079Czo2p2 39.6 0.02 28.55 0 6.79 0.06 0.12 0 23.85 0.03 0 99.02 3.035 0.001 2.579 0 0.391 0.004 0.008 0 1.958 0.004 0 7.981 13.16498316 T.S. Block LNGT001 282.000 1554.87 0.00333M400_079Czo2p3 39.48 0 28.55 0.02 4.9 1.44 0.22 0.01 24.41 0 0 99.06 3.035 0 2.588 0.001 0.284 0.093 0.014 0.001 2.013 0 0 8.029 9.888579387 T.S. Block LNGT001 282.000 1554.87 0.00333M400_083Ep1p1 38.5 0.01 21.71 0.09 15.77 0.14 0.09 0 22.87 0 0 99.2 3.045 0.001 2.024 0.006 0.938 0.009 0.006 0 1.94 0 0 7.97 31.66779203M400_083Ep1p2 38.53 0.04 21.03 0.05 16.59 0.15 0.07 0.01 22.61 0 0 99.1 3.057 0.002 1.967 0.003 0.991 0.01 0.005 0.001 1.924 0 0 7.96 33.50236646M400_083Ep1p3 37.94 0 20.76 0.02 16.31 0.33 0.05 0 23.15 0.01 0.03 98.6 3.037 0 1.959 0.001 0.982 0.022 0.003 0 1.985 0.002 0.003 7.995 33.3900034M400_083Ep2p1 38.39 0 22.36 0.08 12.26 1.74 0.14 0.01 23.59 0.03 0.01 98.62 3.053 0 2.097 0.005 0.734 0.116 0.009 0.001 2.01 0.005 0.001 8.032 25.92723419M400_083Ep2p2 38.43 0 22.5 0.04 14.62 0.13 0.11 0.02 23.36 0 0 99.24 3.031 0 2.092 0.002 0.868 0.009 0.007 0.002 1.976 0 0 7.988 29.32432432M400_083Ep2p3 38.54 0.05 22.6 0.04 13.96 0.59 0.24 0.02 23.37 0.02 0 99.43 3.035 0.003 2.098 0.002 0.827 0.039 0.016 0.002 1.972 0.003 0 7.999 28.27350427
M400_088Czo1p1 38.61 0.05 25.52 0.01 10.35 0.09 0.12 0.02 23.41 0 0 98.21 3.027 0.003 2.359 0.001 0.611 0.006 0.008 0.002 1.969 0 0 7.985 20.57239057 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Czo1p2 38.97 0.04 25.97 0 7.48 1.56 0.14 0.02 23.86 0.03 0 98.07 3.056 0.002 2.401 0 0.441 0.102 0.009 0.002 2.005 0.005 0 8.023 15.51724138 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Czo1p3 39.08 0 26.63 0.01 7.98 0.57 0.08 0.02 23.77 0.01 0 98.15 3.047 0 2.448 0.001 0.468 0.037 0.005 0.002 1.986 0.002 0 7.996 16.04938272 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Czo1p4 39.35 0 28.14 0 5.05 1.43 0.11 0.03 24.25 0.02 0.01 98.4 3.045 0 2.568 0 0.294 0.093 0.007 0.003 2.011 0.003 0.001 8.026 10.27253669 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Czo1p5 38.68 0.04 27.07 0.04 7.65 0.79 0.11 0.03 23.95 0.01 0 98.38 3.013 0.002 2.486 0.002 0.449 0.052 0.007 0.003 1.999 0.002 0 8.016 15.29812606 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep1p1 38.26 0.02 23.32 0.08 12.66 0.65 0.08 0 23.49 0.01 0 98.57 3.028 0.001 2.176 0.005 0.754 0.043 0.005 0 1.992 0.002 0 8.005 25.7337884 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep1p2 38.16 0 22.93 0.06 12.98 0.78 0.07 0 23.54 0 0 98.54 3.028 0 2.145 0.004 0.775 0.052 0.005 0 2.003 0 0 8.011 26.54109589 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep1p3 38.45 0.01 23.41 0.07 11.62 1.12 0.06 0.02 23.54 0 0.02 98.31 3.047 0.001 2.187 0.004 0.693 0.074 0.004 0.002 1.999 0 0.002 8.012 24.0625 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep2p1 37.9 0 22.16 0.01 12.23 1.83 0.08 0 23.65 0 0 97.88 3.041 0 2.097 0.001 0.739 0.123 0.005 0 2.036 0 0 8.041 26.05782793 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep2p2 38.4 0.02 22.99 0 11.99 1.28 0.08 0 23.62 0.03 0 98.41 3.048 0.001 2.151 0 0.716 0.085 0.005 0 2.009 0.005 0 8.02 24.97384025 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep2p3 37.88 0 23.17 0 11.39 1.79 0.09 0.03 23.88 0 0.01 98.24 3.02 0 2.178 0 0.683 0.12 0.006 0.004 2.04 0 0.001 8.05 23.87277176 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep3p1 38.24 0 23.42 0.06 11.23 1.4 0.08 0.02 23.6 0.04 0 98.1 3.04 0 2.195 0.004 0.672 0.093 0.005 0.002 2.01 0.006 0 8.028 23.43913498 T.S. Block MCD0362 910.900 1548.07 0.00238
A-9
M400_088Ep3p2 38.81 0.03 24.19 0.02 10.73 1.29 0.08 0 23.9 0 0 99.07 3.044 0.002 2.237 0.001 0.633 0.084 0.005 0 2.011 0 0 8.018 22.05574913 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep3p3 38.34 0.04 23.27 0.07 12.16 1.07 0.05 0.03 23.57 0.02 0.01 98.64 3.034 0.002 2.171 0.004 0.724 0.071 0.003 0.004 1.998 0.003 0.001 8.016 25.00863558 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep4p1 38.65 0.02 23.82 0.11 9.91 2.05 0.04 0.01 23.88 0.01 0.01 98.51 3.055 0.001 2.22 0.007 0.589 0.136 0.003 0.001 2.023 0.002 0.001 8.037 20.96831613 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep4p2 38.51 0 23.79 0.16 9.83 2.15 0.07 0.01 23.86 0 0 98.4 3.05 0 2.221 0.01 0.586 0.142 0.005 0.001 2.027 0 0 8.042 20.87638048 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep4p3 38.36 0.02 23.58 0.11 10.29 1.64 0.06 0.01 23.51 0 0 97.6 3.057 0.001 2.215 0.007 0.617 0.109 0.004 0.001 2.01 0 0 8.022 21.78672316 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep5p1 38.24 0.05 23.64 0.09 10.88 1.55 0.08 0 23.68 0 0 98.23 3.035 0.003 2.212 0.006 0.65 0.103 0.005 0 2.016 0 0 8.029 22.71139064 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep5p2 38.32 0.03 23.76 0.12 11.22 1.39 0.21 0.01 23.65 0 0 98.74 3.027 0.002 2.213 0.007 0.667 0.092 0.014 0.001 2.004 0 0 8.027 23.15972222 T.S. Block MCD0362 910.900 1548.07 0.00238M400_088Ep5p3 38.31 0.02 22.83 0.13 12.65 1.23 0.07 0.01 23.6 0.02 0 98.88 3.033 0.001 2.131 0.008 0.754 0.082 0.005 0.001 2.002 0.003 0 8.02 26.13518198 T.S. Block MCD0362 910.900 1548.07 0.00238M400_089Ep1p1 38.22 0.11 22.11 0.02 11.96 2.13 0.1 0.02 23.58 0 0 98.27 3.054 0.007 2.083 0.001 0.719 0.142 0.007 0.002 2.021 0 0 8.037 25.66024268M400_089Ep1p2 37.81 0.06 21.57 0.01 12.42 2.17 0.07 0.01 23.54 0 0 97.68 3.049 0.004 2.051 0.001 0.753 0.146 0.005 0.001 2.036 0 0 8.045 26.85449358M400_089Ep1p3 37.9 0.06 22.79 0.01 14.05 0.13 0.14 0 23.16 0.03 0.01 98.28 3.015 0.004 2.137 0.001 0.841 0.008 0.009 0 1.974 0.005 0.001 7.995 28.24042982M400_095Ep1pt1 38.17 0 22.76 0 12.9 0.98 0.16 0.01 23.55 0 0 98.56 3.032 0 2.131 0 0.771 0.065 0.011 0.001 2.006 0 0 8.017 26.56788422M400_095Ep1pt2 38 0.08 22.36 0 12.25 1.53 0.17 0 23.36 0.01 0 97.76 3.046 0.005 2.113 0 0.739 0.102 0.012 0 2.006 0.002 0 8.024 25.91164095M400_095Ep1pt3 38.22 0.08 22.75 0 13.9 0.42 0.16 0.02 23.34 0.02 0 98.91 3.023 0.005 2.121 0 0.828 0.028 0.011 0.002 1.978 0.003 0 7.999 28.07731434M400_095Ep2pt1 38.22 0.12 22.48 0 12.19 1.37 0.14 0.01 23.26 0 0 97.81 3.055 0.007 2.119 0 0.734 0.092 0.009 0.001 1.994 0 0 8.011 25.72730459M400_095Ep2pt2 38.22 0.01 22.12 0.02 15.23 0.14 0.13 0 23.33 0 0 99.22 3.023 0.001 2.063 0.001 0.906 0.009 0.009 0 1.979 0 0 7.991 30.51532503M400_095Ep2pt3 38.34 0.05 22.88 0 14.27 0.13 0.2 0 23.3 0.01 0 99.18 3.022 0.003 2.126 0 0.846 0.009 0.013 0 1.968 0.002 0 7.989 28.46567968M400_095Ep3pt1 38.5 0.06 22.91 0 14.47 0.13 0.12 0 23.54 0 0 99.75 3.019 0.004 2.118 0 0.854 0.009 0.008 0 1.98 0 0 7.991 28.73485868M400_095Ep3pt2 38.43 0.07 22.78 0.01 14.48 0.13 0.2 0.01 23.3 0 0 99.43 3.023 0.004 2.113 0.001 0.857 0.009 0.013 0.001 1.966 0 0 7.987 28.85521886M400_095Ep3pt3 38.17 0.04 22.6 0.01 12.68 1.37 0.14 0.02 23.62 0 0 98.67 3.033 0.002 2.117 0.001 0.758 0.091 0.009 0.002 2.013 0 0 8.027 26.36521739M400_098Czo1p1 39.48 0.03 28.75 0 6.49 0.06 0.09 0.16 23.51 0.07 0.08 98.72 3.03 0.002 2.602 0 0.375 0.004 0.006 0.018 1.934 0.01 0.008 7.989 12.59657373 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Czo1p2 39.46 0 27.73 0 7.87 0.07 0.05 0.06 23.65 0.02 0.02 98.93 3.037 0 2.516 0 0.456 0.005 0.003 0.007 1.95 0.003 0.002 7.979 15.34320323 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Czo1p3 39.81 0 27.81 0 7.6 0.07 0.1 0.12 23.53 0.1 0.03 99.17 3.052 0 2.514 0 0.439 0.004 0.006 0.014 1.933 0.015 0.003 7.98 14.86623772 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Czo2p1 39.75 0 29.61 0 5.47 0.05 0.16 0.04 24.19 0 0 99.29 3.026 0 2.657 0 0.313 0.003 0.01 0.005 1.975 0 0 7.989 10.53872054 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Czo2p2 39.93 0 30.05 0 5.01 0.05 0.16 0.02 24.28 0.03 0 99.52 3.027 0 2.685 0 0.286 0.003 0.01 0.002 1.972 0.004 0 7.99 9.626388421 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Czo2p3 39.85 0 29.49 0 5.47 0.24 0.1 0 24.38 0.01 0 99.54 3.029 0 2.643 0 0.313 0.015 0.006 0 1.986 0.001 0 7.994 10.58863329 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Ep1p1 38.83 0.04 23.86 0.14 11.27 1.35 0.1 0 23.8 0 0 99.41 3.042 0.002 2.204 0.009 0.665 0.088 0.007 0 2 0 0 8.017 23.17880795 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Ep1p2 38.71 0.03 24.22 0.1 12.09 0.43 0.11 0.01 23.6 0.02 0 99.32 3.027 0.002 2.233 0.006 0.712 0.028 0.007 0.001 1.978 0.003 0 7.997 24.17657046 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Ep1p3 38.92 0.08 24.12 0.4 11.1 1.2 0.12 0 23.42 0 0 99.39 3.044 0.005 2.224 0.025 0.653 0.078 0.008 0 1.964 0 0 8.001 22.69725408 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Ep2p1 39.01 0.04 23.68 0.17 11.3 1.41 0.08 0.02 23.72 0 0 99.46 3.055 0.002 2.186 0.011 0.666 0.092 0.005 0.002 1.992 0 0 8.012 23.35203366 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Ep2p2 38.82 0.01 24.43 0.02 12.37 0.11 0.11 0.01 23.55 0 0 99.45 3.027 0.001 2.246 0.001 0.726 0.007 0.007 0.001 1.97 0 0 7.986 24.42799462 T.S. Block MCD0393 193.700 1548.08 0.00359M400_098Ep2p3 38.96 0.05 24.57 0.01 11.83 0.28 0.07 0 23.74 0.01 0 99.53 3.033 0.003 2.255 0.001 0.693 0.018 0.005 0 1.98 0.002 0 7.99 23.50746269 T.S. Block MCD0393 193.700 1548.08 0.00359
M400_106Czo1p1 39.88 0 29.77 0.02 5.37 0.05 0.2 0.03 24.05 0 0 99.39 3.03 0 2.666 0.001 0.307 0.003 0.013 0.003 1.96 0 0 7.983 10.32626976M400_106Czo1p2 39.75 0 30.02 0 3.36 1 0.1 0.02 24.46 0.02 0 98.74 3.038 0 2.705 0 0.193 0.064 0.006 0.002 2.003 0.003 0 8.015 6.659765355M400_106Czo1p3 39.64 0 30.36 0 2.33 1.23 0.11 0.01 24.45 0.01 0.01 98.15 3.041 0 2.746 0 0.135 0.079 0.007 0.001 2.01 0.001 0.001 8.02 4.685872961M400_106Ep1p1 38.84 0 23.8 0 12.47 0.3 0.1 0.01 23.56 0 0.01 99.09 3.045 0 2.2 0 0.735 0.02 0.007 0.001 1.979 0 0.001 7.988 25.04258944M400_106Ep1p2 39.07 0.02 25.34 0.02 9.49 0.98 0.13 0.03 23.82 0 0.01 98.91 3.048 0.001 2.331 0.001 0.557 0.064 0.009 0.003 1.991 0 0.001 8.007 19.2867036M400_106Ep1p3 38.84 0 26.29 0.03 9.56 0.09 0.11 0.03 23.69 0 0 98.66 3.023 0 2.412 0.002 0.56 0.006 0.007 0.003 1.977 0 0 7.99 18.84253028
M400_109Czo1p1 40.42 0.02 31.44 0.03 1.86 0.51 0.14 0.02 24.32 0 0 98.79 3.057 0.001 2.803 0.002 0.106 0.032 0.009 0.002 1.973 0 0 7.986 3.643863871M400_109Czo1p2 40.01 0 30.54 0 3.68 0.32 0.15 0 24.37 0 0 99.09 3.036 0 2.732 0 0.21 0.02 0.01 0 1.984 0 0 7.992 7.13800136M400_109Czo1p3 39.99 0 31.34 0.03 1.86 0.82 0.28 0.02 24.39 0 0.01 98.74 3.036 0 2.805 0.002 0.106 0.052 0.018 0.002 1.984 0 0.001 8.007 3.641360357M400_109Czo1p4 39.91 0 30.27 0 3.49 0.61 0.24 0.02 24.26 0 0 98.82 3.041 0 2.719 0 0.2 0.039 0.015 0.002 1.983 0 0 7.999 6.851661528M400_109Czo1p5 40.33 0.03 30.42 0 3.76 0.03 0.16 0 23.81 0.17 0 98.72 3.063 0.002 2.724 0 0.215 0.002 0.01 0 1.938 0.025 0 7.979 7.315413406M400_109Czo1p6 40.31 0 31.26 0 1.91 0.75 0.13 0.02 24.39 0.1 0.01 98.88 3.053 0 2.791 0 0.109 0.048 0.008 0.002 1.979 0.015 0.001 8.005 3.75862069M400_109Ep1p1 38.96 0.01 24.23 0.02 12.36 0.11 0.09 0.02 23.57 0 0.01 99.38 3.04 0.001 2.229 0.001 0.725 0.007 0.006 0.002 1.97 0 0.001 7.983 24.54299255M400_109Ep1p2 38.62 0.01 22.97 0 14.29 0.13 0.17 0.07 23.04 0 0.03 99.33 3.035 0.001 2.128 0 0.845 0.009 0.011 0.008 1.94 0 0.003 7.98 28.42246889M400_109Ep1p3 39.08 0.02 25.34 0 9.92 0.53 0.08 0.02 23.68 0.02 0 98.69 3.051 0.001 2.332 0 0.583 0.035 0.005 0.002 1.981 0.003 0 7.992 20
M400_115Czo1p1 38.55 0.49 26.01 0.03 4.25 4.08 0.04 0.06 24.05 0 0 97.59 3.05 0.029 2.426 0.002 0.253 0.27 0.003 0.007 2.041 0 0 8.081 9.443822322 T.S. Block CD10628 444.310 1556.22 0.01745M400_115Czo1p2 38.62 0.27 25.59 0 4.39 4.01 0.04 0.07 24.11 0 0 97.12 3.071 0.016 2.399 0 0.262 0.267 0.003 0.008 2.056 0 0 8.082 9.845922585 T.S. Block CD10628 444.310 1556.22 0.01745M400_115Czo1p3 38.75 0.05 27.07 0 5.92 1.8 0.06 0 24.22 0 0 97.9 3.034 0.003 2.498 0 0.349 0.118 0.004 0 2.034 0 0 8.04 12.25851774 T.S. Block CD10628 444.310 1556.22 0.01745M400_115Czo1p4 38.93 0.02 28.39 0.03 4.15 1.86 0.15 0.02 24.3 0.02 0 97.88 3.03 0.001 2.605 0.002 0.243 0.121 0.01 0.002 2.027 0.003 0 8.045 8.532303371 T.S. Block CD10628 444.310 1556.22 0.01745M400_115Czo1p5 38.73 0.03 28.06 0.01 3.91 2.34 0.11 0.03 24.41 0 0.02 97.65 3.029 0.002 2.587 0.001 0.23 0.153 0.007 0.003 2.046 0 0.002 8.061 8.164714235 T.S. Block CD10628 444.310 1556.22 0.01745M400_115Czo1p6 38.84 0.16 28.39 0.01 3.31 2.36 0.07 0.04 24.24 0.01 0 97.43 3.035 0.009 2.616 0.001 0.195 0.155 0.005 0.005 2.03 0.002 0 8.051 6.937033084 T.S. Block CD10628 444.310 1556.22 0.01745M400_115Czo1p7 39.3 0.11 29.21 0.01 3.86 1.03 0.06 0.03 24 0 0 97.63 3.042 0.006 2.666 0.001 0.225 0.067 0.004 0.003 1.993 0 0 8.006 7.782774127 T.S. Block CD10628 444.310 1556.22 0.01745M400_122Czo1pt1 39.23 0.1 27.23 0.03 7.51 0.53 0.23 0 23.68 0.02 0 98.56 3.04 0.006 2.488 0.002 0.438 0.034 0.015 0 1.966 0.003 0 7.992 14.96924129M400_122Czo1pt2 39.25 0.11 27.35 0.01 8.08 0.07 0.2 0.01 23.47 0 0.01 98.56 3.037 0.006 2.495 0.001 0.47 0.005 0.013 0.001 1.946 0 0.001 7.975 15.85160202M400_122Czo1pt3 39.42 0.12 27.5 0 7.47 0.44 0.22 0.01 23.79 0 0 98.99 3.039 0.007 2.499 0 0.433 0.028 0.014 0.001 1.967 0 0 7.988 14.7680764M400_122Czo2pt1 39.02 0.18 26.83 0.07 5.58 1.9 0.23 0.04 23.51 0.07 0.01 97.44 3.063 0.011 2.483 0.004 0.33 0.125 0.015 0.005 1.977 0.011 0.001 8.024 11.73124778M400_122Czo2pt2 39.03 0.07 27.38 0.07 6.52 1.18 0.28 0.02 23.84 0.01 0.01 98.41 3.033 0.004 2.509 0.004 0.381 0.077 0.018 0.002 1.985 0.002 0.001 8.017 13.183391M400_122Czo2pt3 39.37 0.14 27.36 0.05 6.79 0.84 0.2 0 23.69 0.01 0.01 98.46 3.05 0.008 2.499 0.003 0.396 0.055 0.013 0 1.967 0.002 0.001 7.994 13.67875648M400_124Czo1pt1 38.4 0.09 24.54 0.08 10.9 0.65 0.25 0.01 23.32 0 0 98.25 3.028 0.005 2.282 0.005 0.647 0.043 0.017 0.001 1.973 0 0 8 22.08945032M400_124Czo1pt2 39.12 0.07 26.25 0.01 9.42 0.11 0.25 0.02 23.49 0.01 0.02 98.77 3.038 0.004 2.404 0.001 0.551 0.007 0.016 0.002 1.955 0.002 0.002 7.982 18.6463621M400_124Czo1pt3 39.32 0.13 27.23 0.05 6.25 1.34 0.21 0 23.82 0.01 0 98.37 3.054 0.008 2.493 0.003 0.365 0.087 0.014 0 1.982 0.002 0 8.008 12.77116865M400_124Czo2pt1 39.2 0 26.66 0.02 8.98 0.22 0.19 0 23.84 0 0.02 99.13 3.032 0 2.431 0.001 0.523 0.014 0.012 0 1.976 0 0.002 7.991 17.70480704M400_124Czo2pt2 38.97 0.07 26.42 0.07 8.72 0.56 0.26 0.02 23.62 0 0 98.73 3.031 0.004 2.422 0.004 0.51 0.036 0.017 0.002 1.97 0 0 7.997 17.39427012M400_124Czo2pt3 39 0.08 26.8 0.03 8.75 0.08 0.16 0 23.6 0 0.01 98.51 3.029 0.005 2.454 0.002 0.511 0.005 0.011 0 1.964 0 0.001 7.983 17.23440135M400_124Czo3pt1 38.17 0.07 23.82 0.04 11.96 0.22 0.27 0 22.97 0.01 0.01 97.54 3.036 0.004 2.234 0.003 0.716 0.015 0.018 0 1.958 0.002 0.001 7.985 24.27118644M400_124Czo3pt2 38.39 0.07 24.01 0.03 12.09 0.31 0.3 0.01 23.22 0.01 0 98.44 3.029 0.004 2.233 0.002 0.718 0.02 0.02 0.001 1.963 0.002 0 7.992 24.33073534M400_124Czo3pt3 38.83 0.11 24.47 0.08 12.22 0.24 0.31 0.01 23.43 0 0.01 99.71 3.023 0.006 2.246 0.005 0.716 0.016 0.02 0.001 1.954 0 0.001 7.988 24.17285618M400_132Czo1p1 39.19 0.01 27.8 0 6.15 0.51 0.12 0.06 23.64 0 0.01 97.49 3.053 0.001 2.553 0 0.36 0.033 0.008 0.007 1.973 0 0.001 7.99 12.35839341M400_132Czo1p2 39.19 0.03 27.59 0.02 7.33 0.07 0.1 0.02 23.65 0 0 98.03 3.042 0.002 2.524 0.001 0.428 0.005 0.007 0.002 1.969 0 0 7.98 14.49864499M400_132Czo1p3 39.28 0 28.18 0 6.06 0.17 0.07 0.04 23.65 0 0.02 97.48 3.052 0 2.582 0 0.355 0.011 0.005 0.005 1.969 0 0.002 7.98 12.08716377M400_140Czo1p1 38.67 0 25.84 0.04 9.58 0.56 0.14 0 23.81 0.02 0.01 98.67 3.021 0 2.38 0.002 0.563 0.036 0.009 0 1.993 0.003 0.001 8.009 19.13013931 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Czo1p2 38.57 0 24.49 0 10.95 0.58 0.09 0.01 23.59 0.02 0 98.3 3.038 0 2.274 0 0.649 0.038 0.006 0.001 1.991 0.003 0 8.001 22.20321587 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Czo1p3 38.64 0.04 22.88 0.01 12.97 0.63 0.06 0.03 23.37 0.01 0 98.64 3.055 0.002 2.132 0.001 0.772 0.042 0.004 0.004 1.98 0.002 0 7.992 26.58402204 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Czo2p1 38.69 0.05 23.97 0 11 1.26 0.11 0.05 23.74 0 0 98.9 3.043 0.003 2.222 0 0.651 0.083 0.007 0.006 2.002 0 0 8.018 22.65924121 T.S. Block HRD0026 156.46-15 1546.98 0.00389
A-1
0
M400_140Czo2p2 38.72 0 24.88 0.01 12.29 0.11 0.61 0.05 22.56 0.01 0 99.24 3.021 0 2.289 0.001 0.722 0.007 0.04 0.006 1.886 0.002 0 7.974 23.9787446 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Czo2p3 38.59 0 24.68 0.03 9.54 1.4 0.11 0.02 23.78 0.01 0 98.17 3.045 0 2.296 0.002 0.567 0.093 0.007 0.002 2.011 0.002 0 8.024 19.80440098 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Ep1p1 38.56 0.08 21.47 0.01 12.19 2.16 0.02 0.04 23.4 0 0.01 97.94 3.091 0.005 2.029 0.001 0.735 0.145 0.001 0.005 2.01 0 0.001 8.022 26.5918958 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Ep1p2 38.42 0.17 21.27 0.02 12.62 2.3 0.04 0.06 23.36 0.01 0.01 98.27 3.077 0.01 2.008 0.001 0.76 0.154 0.003 0.007 2.005 0.002 0.001 8.029 27.4566474 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Ep1p3 38.29 0 22.22 0.02 14.72 0.13 0.04 0.01 23.2 0 0 98.66 3.038 0 2.078 0.001 0.879 0.009 0.003 0.001 1.974 0 0 7.983 29.72607372 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Ep2p1 38.37 0.02 21.48 0.02 14.76 1.02 0.08 0.02 23.5 0.04 0 99.31 3.043 0.001 2.008 0.001 0.881 0.067 0.005 0.002 1.997 0.006 0 8.013 30.49498096 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Ep2p2 38.35 0.02 21.59 0 15.81 0.14 0.08 0.02 23.25 0.02 0 99.28 3.036 0.001 2.015 0 0.942 0.01 0.005 0.002 1.972 0.003 0 7.986 31.85661143 T.S. Block HRD0026 156.46-15 1546.98 0.00389M400_140Ep2p3 38.29 0.06 21.79 0 14.81 0.79 0.09 0.08 23.41 0.02 0 99.33 3.032 0.004 2.034 0 0.882 0.052 0.006 0.009 1.986 0.003 0 8.008 30.24691358 T.S. Block HRD0026 156.46-15 1546.98 0.00389
WB116Ep1p1 38.48 0 23.05 0 14.34 0.13 0.73 0.03 21.12 0.01 0.01 97.9 3.057 0 2.159 0 0.857 0.009 0.049 0.004 1.798 0.002 0.001 7.936 28.41511936 T.S. Block WB0801CD 116 1542.35 0.00374WB116Ep1p2 38.12 0.02 23.6 0 12.18 0.11 0.15 0.01 22.18 0.01 0 96.38 3.059 0.001 2.233 0 0.736 0.007 0.01 0.001 1.907 0.002 0 7.956 24.78949141 T.S. Block WB0801CD 116 1542.35 0.00374WB116Ep1p3 38.41 0.07 22.67 0 13.98 0.13 0.16 0.01 21.58 0 0 97.03 3.074 0.004 2.139 0 0.842 0.009 0.011 0.001 1.852 0 0 7.932 28.24555518 T.S. Block WB0801CD 116 1542.35 0.00374
WB377_5Czo1p1 39.38 0 28.22 0.03 6.96 0.06 0.2 0.05 23.62 0 0 98.55 3.035 0 2.564 0.002 0.404 0.004 0.013 0.006 1.952 0 0 7.98 13.61185984WB377_5Czo1p2 39.04 0.08 27.52 0.01 5.06 2.13 0.16 0.08 24.21 0 0 98.31 3.039 0.005 2.525 0.001 0.296 0.139 0.011 0.009 2.021 0 0 8.045 10.49273307WB377_5Czo1p3 39.43 0.11 28.12 0.02 6.32 0.71 0.24 0.04 23.86 0 0.03 98.87 3.036 0.006 2.553 0.001 0.366 0.046 0.016 0.005 1.969 0 0.003 7.999 12.5385406WB377_5Czo2p1 39.02 0.12 27.73 0.04 6.83 0.59 0.27 0.05 23.63 0 0.01 98.29 3.027 0.007 2.536 0.002 0.399 0.038 0.018 0.006 1.964 0 0.001 7.998 13.59454855WB377_5Czo2p2 39.11 0.08 27.76 0.02 7.2 0.07 0.23 0.04 23.47 0.02 0 97.99 3.035 0.005 2.54 0.001 0.42 0.004 0.015 0.005 1.952 0.003 0 7.981 14.18918919WB377_5Czo2p3 39.31 0.12 27.86 0 7.17 0.33 0.39 0.04 23.62 0 0 98.86 3.03 0.007 2.532 0 0.416 0.021 0.025 0.005 1.953 0 0 7.989 14.11126187WB377_5Czo3p1 38.71 0.03 24.47 0.01 9.37 1.46 0.21 0.02 23.51 0 0.05 97.84 3.063 0.002 2.283 0.001 0.558 0.096 0.014 0.002 1.993 0 0.005 8.017 19.64097149WB377_5Czo3p2 38.97 0 24.61 0.04 11.48 0.1 0.16 0.03 22.73 0 0.02 98.14 3.062 0 2.28 0.002 0.678 0.007 0.011 0.004 1.914 0 0.002 7.959 22.92089249WB377_5Czo3p3 38.71 0 24.84 0.02 11.34 0.1 0.1 0.02 23.54 0 0.03 98.71 3.031 0 2.293 0.001 0.668 0.007 0.007 0.002 1.975 0 0.003 7.989 22.55994596WB377_5Ep1p1 38.81 0.03 24.68 0.04 11.32 0.1 0.24 0.02 22.92 0 0.02 98.18 3.051 0.002 2.287 0.002 0.67 0.007 0.016 0.002 1.93 0 0.002 7.969 22.65809943WB377_5Ep1p2 38.58 0.03 24.71 0 11.46 0.1 0.22 0.02 23.26 0 0.01 98.4 3.032 0.002 2.289 0 0.678 0.007 0.015 0.002 1.958 0 0.001 7.984 22.85136502WB377_5Ep1p3 38.77 0.03 24.52 0 10.97 0.46 0.2 0.01 23.41 0 0.02 98.39 3.048 0.002 2.273 0 0.649 0.03 0.013 0.001 1.972 0 0.002 7.99 22.21081451WB470_8Ep4p1 37.98 0.02 20.94 0.05 15.39 0.7 0.32 0.01 22.94 0 0 98.38 3.045 0.001 1.979 0.003 0.929 0.047 0.022 0.001 1.972 0 0 7.999 31.94635488 T.S. Block WB0801CD 470 1545.63 0.00651WB470_8Ep4p2 38.05 0.03 21.61 0.01 15.29 0.14 0.29 0.04 22.82 0.01 0 98.29 3.039 0.002 2.035 0.001 0.919 0.009 0.02 0.005 1.953 0.002 0 7.983 31.11035884 T.S. Block WB0801CD 470 1545.63 0.00651WB470_8Ep4p3 38.05 0.07 21.72 0.02 14.12 1 0.32 0.03 23.1 0.02 0 98.45 3.039 0.004 2.045 0.001 0.849 0.067 0.022 0.004 1.977 0.003 0 8.011 29.3365584 T.S. Block WB0801CD 470 1545.63 0.00651WB470_8Ep4p4 38.74 0 24.14 0.03 11.77 0.11 0.14 0.02 23.18 0 0 98.15 3.053 0 2.243 0.002 0.698 0.007 0.009 0.002 1.96 0 0 7.975 23.73342401 T.S. Block WB0801CD 470 1545.63 0.00651
Epidote-Clinozoisite (Bil)Sample Number SiO2 TiO2 Al2O3 Cr2O3 Fe2O3 FeO MnO MgO CaO Na2O K2O totals Si Ti Al Cr Fe3+ Fe2+
Mn Mg Ca Na K totals Fe 3+ /(Fe 3+ +Al)*100 Sample HoleID Depth W1550 D1550CD2425 254.5m 2A-01 39.06 0 24.62 0.42 13.33 0.12 0 0 23.79 0 0 101.37 2.999 0 2.228 0.025 0.77 0.008 0 0 1.959 0 0 7.989 25.68378919
CD2425_334_3A-a 38.41 0 25.15 0 10.27 2.11 0.2 0.18 24.71 0 0 101.05 2.971 0 2.294 0 0.598 0.136 0.013 0.021 2.05 0 0 8.083 20.67773167 T.S. Block Cd2425 334 1545.99 0.0129CD2425_334_3B-a 37.68 0 23.64 0.28 12.45 2.34 0 0.07 24.78 0 0 101.27 2.94 0 2.175 0.017 0.731 0.153 0 0.008 2.074 0 0 8.098 25.15485203 T.S. Block Cd2425 334 1545.99 0.0129CD2425 334m 3B-c 38.46 0 26.11 0 7.42 3.2 0.35 0.05 25.15 0 0 100.77 2.977 0 2.383 0 0.432 0.207 0.023 0.006 2.088 0 0 8.116 15.34635879 T.S. Block Cd2425 334 1545.99 0.0129CD2425_334_3C-b 37.45 0 26.14 0 10.9 1.32 0.33 0.09 24.88 0 0 101.13 2.896 0 2.383 0 0.634 0.085 0.022 0.01 2.064 0 0 8.095 21.01425257 T.S. Block Cd2425 334 1545.99 0.0129
CD2425 547m 65A-04 38.74 2.3 25.27 0 4.26 6.58 0 0.12 23.15 0 0 100.45 3.009 0.134 2.314 0 0.249 0.428 0 0.014 1.928 0 0 8.076 9.715177526CD5653 389.8m 59A-01 38.68 0 26.73 0 13.16 0.12 0 0.32 22.3 0 0 101.33 2.949 0 2.402 0 0.755 0.008 0 0.036 1.823 0 0 7.973 23.91510928CD5653 389.8m 59A-02 38.77 0.69 26.33 0 12.2 0.11 0 0 22.65 0 0.48 101.23 2.963 0.04 2.372 0 0.702 0.007 0 0 1.855 0 0.047 7.984 22.83669486CD5653 389.8m 59A-03 39.08 0 25.59 0 13.2 0.12 0 0 23.33 0 0 101.35 2.989 0 2.307 0 0.76 0.008 0 0 1.914 0 0 7.978 24.77991523CD5653 389.8m 59B-01 39.37 0 26.63 0 13.11 0.12 0 0.36 21.72 0 0 101.34 2.99 0 2.385 0 0.75 0.008 0 0.041 1.769 0 0 7.942 23.92344498CD5653 389.8m 59B-02 37.58 0.84 26.64 0 13.61 0.12 0 0.45 22.13 0 0 101.4 2.875 0.048 2.402 0 0.783 0.008 0 0.051 1.816 0 0 7.984 24.58398744CD5653 389.8m 59B-03 39.54 0.73 25.46 0 13.36 0.12 0 0 22.13 0 0 101.36 3.012 0.042 2.286 0 0.766 0.008 0 0 1.808 0 0 7.921 25.0982962CD6024 350.9m 47A-01 39.08 0.23 25.79 0 13.25 0.12 0 0.21 22.65 0 0 101.35 2.983 0.013 2.321 0 0.761 0.008 0 0.024 1.854 0 0 7.963 24.6917586CD6024 350.9m 47A-07 39.4 0.49 27.28 0 10.55 0.1 0 0.13 23.12 0 0 101.09 2.989 0.028 2.44 0 0.602 0.006 0 0.015 1.881 0 0 7.962 19.7896121CD6024 350.9m 47B-02 39.91 1.2 24.4 0 11.31 1.47 0 0.26 22.59 0 0 101.16 3.053 0.069 2.201 0 0.651 0.094 0 0.03 1.854 0 0 7.952 22.82608696CD7063 135m 12A-01 40.07 0.36 27.83 0 5.96 1.87 0 0 24.5 0 0 100.62 3.045 0.021 2.494 0 0.341 0.119 0 0 1.997 0 0 8.017 12.02821869
CD7069 422.7m 28A-01 39.63 0.26 25.88 0 12.52 0.11 0 0.22 22.38 0.07 0.17 101.24 3.018 0.015 2.324 0 0.718 0.007 0 0.025 1.826 0.01 0.017 7.96 23.60289283CD7069 448.5m 34A-08 39.77 0.39 24.64 0 14.24 0.13 0 0 22.09 0 0.17 101.43 3.038 0.022 2.219 0 0.818 0.008 0 0 1.808 0 0.017 7.93 26.93447481CD7069 448.5m 34B-04 40.2 0.4 23.99 0 15.41 0.14 0 0.16 21.25 0 0 101.58 3.065 0.023 2.156 0 0.884 0.009 0 0.018 1.738 0 0 7.892 29.07894737CD7083 375.8m 37A-01 42.88 0 26.85 0 10.31 0.09 0 0.19 20.02 0.69 0 101.03 3.203 0 2.364 0 0.579 0.006 0 0.021 1.602 0.1 0 7.876 19.67380224CD7083 375.8m 37A-02 41.72 0 26.92 0 11.39 0.1 0 0.21 20.67 0.12 0 101.13 3.131 0 2.382 0 0.643 0.006 0 0.023 1.662 0.017 0 7.865 21.25619835CD7083 375.8m 37A-03 42.32 0 27.01 0 10.14 0.09 0 0.15 21.11 0.18 0 101.01 3.169 0 2.384 0 0.572 0.006 0 0.017 1.694 0.026 0 7.867 19.35047361
Numbers of ions on the basis of 12.5 O
A-1
1
Appendix 2: Multi-element geochemistry
A-12
APPENDIX 2Sample Hole_ID depth (m) thin section Ag Al As Ba Be Bi Ca Cd Ce Co Cr Cs Cu Fe Ga Ge Hf In K La Li Mg Mn Mo Na Nb Ni P Pb Rb Re S Sb Sc Se Sn Sr Ta Te Th Ti Tl U V W Y Zn Zr
Number ppm % ppm ppm ppm ppm % ppm ppm ppm ppm ppm ppm % ppm ppm ppm ppm % ppm ppm % ppm ppm % ppm ppm ppm ppm ppm ppm % ppm ppm ppm ppm ppm ppm ppm ppm % ppm ppm ppm ppm ppm ppm ppmJ58791 UDD1420 0.891 0.06 3.89 <0.2 10 0.38 0.06 6.03 0.16 12.7 74.2 212 0.31 34.2 7.79 10.3 1.01 1 0.069 0.07 5.2 21.8 10.55 1270 0.76 0.36 3.1 433 420 2.9 0.8 0.005 0.03 0.29 82.5 1 0.7 10.4 0.23 <0.05 1.4 0.411 0.03 0.2 315 7.2 22.4 91 28.6J58792 UDD1420 4.584 0.09 6.7 6.7 30 0.3 0.03 6.47 0.1 8.81 47.8 123 0.15 142.5 7.61 15.45 0.36 0.5 0.056 0.07 3.5 14.3 4.35 1440 0.3 2.18 3.3 76.2 330 2.6 0.4 0.002 0.13 0.27 50.1 1 0.6 166.5 0.22 0.06 0.6 0.555 0.02 0.1 286 5.6 17.8 97 13.7J58793 UDD1420 56.311 0.03 2.97 56.3 30 0.08 <0.01 3.91 0.08 2.61 93.4 1460 9.03 25.1 6.29 6.62 0.29 0.2 0.02 0.23 1.1 13.5 15 1180 0.15 0.03 0.8 1050 90 1.5 15.8 <0.002 0.03 0.56 21.8 1 0.2 60 0.06 <0.05 0.2 0.152 0.15 <0.1 111 0.6 5 73 4.7J58794 UDD1420 65.263 0.02 2.71 292 10 <0.05 <0.01 5.99 0.09 1.97 89.6 1170 2.08 11 6.11 5.86 0.16 0.1 0.016 0.02 0.7 8.8 14.55 1400 0.21 0.01 0.5 1070 30 3.2 2.1 0.002 0.03 0.71 20.8 1 <0.2 97.8 <0.05 <0.05 <0.2 0.147 0.03 <0.1 105 3.1 6.1 56 1.8J58795 UDD1420 72.217 0.12 2.62 10.2 10 <0.05 <0.01 3.91 0.26 2.9 95 1130 1.38 247 7.39 6.34 0.44 0.1 0.03 0.03 1.1 6.1 15.9 1140 0.2 <0.01 0.6 1260 110 2.1 1.9 0.002 0.17 0.21 20.6 1 0.2 54.9 0.05 0.05 <0.2 0.147 0.03 <0.1 110 0.4 7.5 196 1.9J58796 UDD1420 78.128 0.04 3 16.6 <10 <0.05 <0.01 2.69 0.1 1 86 1660 1.69 26.3 7.09 6.64 0.46 <0.1 0.02 0.01 <0.5 7.6 15.9 1010 0.13 <0.01 0.4 1230 180 1.7 1 <0.002 0.07 0.27 23.9 1 0.2 50.3 <0.05 <0.05 <0.2 0.161 0.02 <0.1 123 0.9 4 113 <0.5J58797 UDD1420 83.378 M400-010 0.03 6.01 12.4 860 0.3 <0.01 1.91 0.07 5.71 72.2 1080 66 4.3 8.26 12.85 0.37 1.2 0.024 4.24 2.4 134.5 12.2 788 0.1 0.4 1.8 627 340 1.7 242 <0.002 0.01 0.35 36.1 1 0.4 6.1 0.13 <0.05 0.4 0.411 2.39 0.1 219 0.5 11.1 104 32.8J58798 UDD1420 83.973 0.03 6.31 1.2 960 0.32 <0.01 1.75 0.04 7 47.8 626 53.8 8 6.91 13 0.22 1.3 0.028 3.79 2.9 123 8.15 833 0.11 2.07 1.8 258 290 2.2 226 <0.002 0.01 0.3 34.5 1 0.7 21.4 0.13 <0.05 0.4 0.431 2.3 0.1 230 0.6 13.1 59 33.2J58799 UDD1420 84.679 0.03 2.65 164 20 0.11 <0.01 6.84 0.22 1.87 71.4 996 2.68 4.2 6.7 6.62 0.18 0.3 0.024 0.1 0.7 13.9 12.5 1470 0.39 0.19 0.7 1080 100 4.1 5.7 <0.002 0.03 1.68 20.7 1 0.4 21.3 <0.05 0.05 <0.2 0.148 0.1 <0.1 99 0.5 5.8 167 9J58800 UDD1420 95.241 0.02 1.21 558 10 <0.05 <0.01 0.59 0.03 0.53 111.5 1120 0.47 18.2 5.49 3.03 0.37 <0.1 0.011 0.01 <0.5 3.1 19.65 934 0.23 <0.01 0.3 2020 20 0.5 0.7 <0.002 0.09 13.2 11.8 1 <0.2 9.8 <0.05 0.08 <0.2 0.071 0.03 <0.1 52 0.6 1.1 50 <0.5J58801 UDD1420 201.159 0.02 1.12 855 <10 <0.05 <0.01 0.96 0.19 0.34 77.9 773 0.29 8.5 4.43 2.72 0.27 <0.1 0.009 0.01 <0.5 1.8 19.75 1070 0.22 <0.01 0.2 1790 20 3.6 0.3 <0.002 0.07 5.62 9.1 1 <0.2 18.4 <0.05 0.07 <0.2 0.047 0.02 <0.1 43 0.8 1.1 210 <0.5J58802 UDD1420 216.077 0.03 4.02 9.7 <10 0.14 <0.01 3.56 0.22 4.91 89.7 1520 1.02 12.6 7.86 8.68 0.38 0.6 0.031 0.03 1.9 3.8 14.6 1110 0.26 0.06 1.2 1060 370 0.9 1.6 <0.002 0.04 2.74 29.6 1 0.4 11.6 0.09 <0.05 0.4 0.281 0.02 0.1 164 0.8 9.7 162 15.4J58803 UDD1420 242.302 M400-011 0.06 5.96 8.2 10 0.38 <0.01 6.59 0.64 6.83 66.6 630 0.2 10.2 7.37 13.3 0.49 0.8 0.037 0.1 3 42.1 8.41 1390 0.47 1.14 2 314 260 16.5 2.5 0.002 0.09 0.55 30.7 1 0.8 64.3 0.13 <0.05 0.7 0.289 0.04 0.2 169 0.4 12.6 569 24.7J58804 UDD1420 244.578 0.03 5.68 86.7 40 0.26 <0.01 6.43 0.1 6.26 58.4 645 0.21 19.5 6.83 13.3 0.64 0.8 0.038 0.11 2.7 48.2 7.23 1180 0.88 1.47 1.5 302 190 1.9 2.7 0.002 0.04 0.58 30.9 1 0.5 112 0.11 <0.05 0.4 0.284 0.02 0.1 174 0.7 12.1 81 25.3J58805 UDD1420 254.54 0.17 6.43 78 140 0.34 <0.01 10.55 1.09 8.55 43.7 343 0.77 45.2 5.83 13.3 0.12 0.5 0.039 0.6 3.7 33.7 3.57 1250 0.54 1.64 2.1 156.5 290 11.6 18 <0.002 0.34 0.61 28.7 1 0.5 151.5 0.13 0.06 0.6 0.326 0.16 0.2 164 2.9 14.6 908 13.3J58806 UDD1420 254.902 M400-012 0.47 7.16 4970 130 0.43 <0.01 7.69 0.25 9.03 63.1 425 0.78 49.7 6.95 15.05 0.24 0.6 0.046 0.6 3.8 41 4.59 1240 0.27 1.93 2.5 216 310 4.5 17.8 0.002 0.79 5.39 35.1 1 0.6 135.5 0.16 0.2 0.7 0.383 0.14 0.2 191 4.7 16 199 16.7J58807 UDD1420 261.024 0.06 6.82 40.6 220 0.45 <0.01 7.74 0.07 8.47 42.7 320 2.39 55.5 4.61 13.9 0.09 0.7 0.033 0.72 3.5 60.2 2.46 991 0.29 1.72 2.4 127 280 2.2 26.6 0.002 0.16 0.29 36.5 1 0.5 148 0.15 0.05 0.6 0.383 0.23 0.1 179 1.6 15 51 22.9J58808 UDD1420 266.946 M400-013 0.06 4.51 37.7 150 0.46 <0.01 6.57 0.1 15.35 68 634 1.77 25.2 8.75 13.25 0.33 1.2 0.07 0.27 6.2 56.2 7.38 1340 0.28 1.14 4.2 397 390 1.7 8.8 <0.002 0.03 0.86 29.2 1 1.3 37 0.24 <0.05 0.5 0.615 0.1 0.1 199 1.8 17.5 127 37.8J58809 UDD1420 267.049 M400-014 0.06 5.15 223 140 0.25 <0.01 4.42 0.07 8.99 87.9 344 4.65 6.5 9.14 14.9 0.57 1.3 0.044 0.57 3.4 110 10.05 1340 0.28 0.28 4.8 369 510 1 26 0.002 0.05 0.52 18.2 1 0.7 16.6 0.31 <0.05 0.4 0.689 0.36 0.1 212 1.4 13.1 114 41.9J58810 UDD1420 268.002 M400-015 0.12 2.84 18.5 <10 0.07 <0.01 4.54 0.05 1.33 90.9 1620 0.3 13.1 6.59 7.59 0.58 0.2 0.026 0.02 <0.5 4.7 14.3 1110 0.13 0.04 0.5 1120 130 0.6 0.5 <0.002 0.02 0.4 12.1 1 0.2 21.3 <0.05 <0.05 <0.2 0.172 0.03 <0.1 126 0.4 5.2 56 2.2J58811 UDD1420 313.893 M400-016 0.05 2.73 221 10 0.06 <0.01 6.8 0.12 2.16 89.6 1160 1.01 50 6.33 6.16 0.24 0.2 0.019 0.02 0.7 5.5 15.35 1550 0.13 0.07 0.4 1180 140 2.6 1.1 <0.002 0.02 3.27 21.6 1 0.2 94.2 <0.05 <0.05 <0.2 0.127 0.02 <0.1 109 0.4 8 70 2.3J58812 UDD1420 314.132 M400-017 0.04 2.47 596 <10 0.07 <0.01 4.52 0.09 1.31 89.8 1240 0.93 29.4 5.81 5.88 0.19 0.1 0.021 0.01 <0.5 4.3 16.45 1290 0.15 0.06 0.4 1600 20 1 0.8 <0.002 0.02 7.74 20.6 1 0.2 53.8 <0.05 0.05 <0.2 0.106 <0.02 <0.1 65 0.4 5.1 63 1.7J58813 UDD1420 324.819 M400-018 0.03 1.94 3.2 <10 0.06 <0.01 3.43 0.07 0.84 92.2 1250 0.88 22.9 5.6 4.71 0.3 0.1 0.016 0.01 <0.5 3.4 16.5 1070 0.16 0.03 0.5 1710 30 1.3 0.8 <0.002 0.04 0.31 18.4 1 0.2 22.3 <0.05 <0.05 <0.2 0.137 0.02 <0.1 67 0.4 3.3 59 1.6J58814 UDD1420 346.176 M400-019 0.02 3.49 3.6 <10 0.07 <0.01 4.25 0.16 0.76 87.2 1790 1.21 24 7.09 8.23 0.36 0.2 0.023 0.02 <0.5 5.7 15 1200 0.11 0.07 0.5 1090 40 0.9 1 <0.002 0.08 0.2 29.6 1 0.2 12.3 <0.05 <0.05 <0.2 0.159 0.03 <0.1 143 0.3 4.8 96 2.1J58815 UDD1420 371.276 0.03 3.12 0.8 <10 0.1 <0.01 5.14 0.1 1.36 96.5 1280 0.39 47.5 6.06 7.33 0.25 0.2 0.022 0.02 0.5 3.2 14.55 1200 0.17 0.09 0.4 1370 30 1.1 0.8 <0.002 0.04 0.2 22.3 1 0.2 35 <0.05 <0.05 <0.2 0.125 0.02 <0.1 119 0.2 5 72 3.3J58816 UDD1420 427.257 0.02 4.08 1.1 <10 0.05 <0.01 4 0.06 1.75 94.4 1500 0.27 73.2 7.07 9.1 0.36 0.3 0.029 0.01 0.6 2.1 13.95 1150 0.12 0.01 0.6 1100 110 <0.5 0.2 0.002 0.13 0.08 31.2 1 <0.2 5.9 <0.05 <0.05 <0.2 0.197 0.04 <0.1 147 0.3 7 61 6.5J58817 UDD1420 440.714 M400-020 0.09 7.16 13.4 230 1.31 <0.01 5.04 0.13 41.1 36.6 59 1.1 46.5 7.73 22.6 0.25 4.8 0.092 0.72 16.4 37.3 2.33 2550 0.84 1.91 9.5 78.7 990 6.6 22.1 0.003 0.17 0.23 34 2 1.8 148 0.62 <0.05 4.3 0.958 0.17 1.3 261 1.3 49.1 123 161.5J58818 UDD1420 444.254 0.08 7.3 3.8 500 1.24 <0.01 2.42 0.13 31.5 39.1 315 0.85 76.2 5.74 20.6 0.16 2.7 0.065 1.24 13.4 41.5 2.4 1320 1.01 1.82 5 198.5 420 10.7 22.5 0.002 0.35 0.12 27.3 1 1.2 198 0.37 <0.05 5 0.463 0.3 1.8 177 0.7 16.3 128 90.4J58819 UDD1420 448.772 0.08 6.05 0.9 220 0.66 0.15 4.55 0.42 44.9 38 290 1.23 82 6.53 16.6 0.15 2.1 0.069 0.81 23.9 37.2 2.68 1170 0.99 0.86 4.3 156.5 410 13 27.7 0.003 0.51 0.22 27.3 2 1.1 167.5 0.29 0.08 5.4 0.468 0.21 0.9 169 1.2 21.3 206 72.2J58820 UDD1420 459.766 M400-021 0.08 6.75 15.2 260 0.56 <0.01 6.46 0.09 8.36 70.5 721 0.56 49.9 7.15 14.2 0.49 0.8 0.043 0.53 3.5 31.2 5.62 1570 0.28 1.96 2 351 290 2.6 18.9 0.002 0.02 0.15 35.7 1 0.6 167.5 0.13 <0.05 0.6 0.339 0.11 0.2 197 0.6 14.9 82 23.6J58821 UDD1420 475.549 M400-022 0.04 2.27 10.2 90 0.27 <0.01 2.22 0.05 7.47 47.5 92 0.45 84.7 2.56 13.05 0.19 0.8 0.038 0.05 3.3 20.6 1.84 539 0.39 0.65 1.8 156.5 100 2 8.3 0.002 0.01 0.43 29 1 0.5 124 0.11 0.05 0.5 0.038 0.06 0.1 25 0.5 17.4 7 23.8J58822 UDD1420 484.906 M400-023 0.04 4.41 30.2 20 0.56 <0.01 7.65 0.1 5.09 84.1 1380 0.47 86.6 7.49 10.4 0.48 0.6 0.039 0.06 2 29.9 10.5 1480 0.14 0.37 0.5 660 130 1.4 2 <0.002 0.06 0.33 33.7 1 0.4 115 <0.05 <0.05 0.2 0.126 0.02 0.1 168 0.4 8.9 80 16J58824 UDD1510 59.1538 M400-025 0.11 6.76 26 80 0.68 <0.01 4.79 0.06 15.5 65.6 45 0.79 110.5 10.1 18.2 0.3 1.6 0.076 0.34 6.3 36.8 3.7 1910 0.42 2.62 5.8 56.1 600 4.6 6.7 0.004 0.29 0.98 50.1 2 0.9 87.1 0.34 0.06 0.8 0.851 0.06 0.2 394 1.4 30.7 95 44.6J58825 UDD1510 143.287 M400-026 0.25 7.4 2310 30 0.76 <0.01 5.98 0.09 16.7 31.2 205 0.21 54.5 8.05 19.45 0.33 1.9 0.119 0.22 7.1 18 4.37 1160 0.53 2.93 4.6 93.6 540 2.5 2.4 0.002 0.46 1.79 34.9 2 1.9 76.7 0.3 0.93 1.7 0.684 0.02 0.5 240 4.1 26.2 134 59.5J58826 UDD1510 144.035 M400-027 0.72 7.42 4490 60 0.74 0.05 6 0.1 16.05 72.7 186 0.37 359 8.96 18.2 0.21 1.3 0.077 0.32 7 24.2 3.25 982 1.14 3.18 4.2 133.5 520 5.5 9.2 0.003 3.24 4 32.1 2 1.3 143 0.27 2.34 1.6 0.619 0.05 0.5 256 19.4 22.1 115 42.2J58827 UDD1510 144.297 0.95 6.06 >10000 70 0.63 0.24 10.75 0.1 16.25 63.8 148 0.31 239 7.69 16.8 0.32 1.2 0.076 0.32 6.9 26.2 3.13 1550 0.46 2.08 3.9 84.2 480 4.9 8.6 0.002 2.46 6.47 28.9 2 1.1 139 0.29 3.98 1.5 0.572 0.08 0.4 221 154.5 25.1 128 37.2J58828 UDD1510 158.067 M400-028 0.16 6.05 56 40 0.33 0.03 10.8 0.12 10.7 37.1 64 0.14 111 6.27 15.35 0.18 0.7 0.05 0.25 4.5 19.6 2.9 1680 0.31 1.41 2.8 47.8 380 1.9 6.4 <0.002 0.12 0.52 35.4 1 0.6 119.5 0.18 0.05 0.8 0.401 0.05 0.2 202 1.2 18.5 78 18.7J58829 UDD1510 169.642 0.26 4.18 492 120 0.26 0.04 5.82 0.07 7.86 36 56 1.09 86.7 5.44 11.35 0.08 0.6 0.031 0.43 3.2 39 1.94 908 1.25 0.9 2.1 45.6 260 1.9 17.1 0.007 1.31 0.31 25.7 2 0.6 54.2 0.14 0.36 0.6 0.311 0.15 0.2 165 11.3 11.9 53 18.1J58830 UDD1510 170.006 M400-029 0.16 5.58 266 120 0.35 0.03 7.18 0.09 10.4 34.7 73 0.9 69.8 6 13.6 0.12 0.7 0.046 0.47 4.3 41.5 2.39 1240 0.53 1.12 2.6 40.6 330 2.6 15 0.003 0.55 0.42 33.6 1 0.6 68.8 0.17 0.21 0.7 0.381 0.13 0.2 186 6.3 16.3 76 18.8J58831 UDD1510 172.565 0.09 7.17 57.8 40 0.41 0.02 7.1 0.09 12.35 42.1 75 0.17 65.6 7.61 17.2 0.47 0.7 0.057 0.32 5 41.2 3.33 1510 0.34 1.5 3.1 49 380 2.1 9.7 <0.002 0.12 0.52 40.9 1 0.7 91.2 0.21 0.05 0.9 0.461 0.08 0.2 232 1.2 20.4 90 19.2J58832 UDD1510 195.829 M400-030 0.14 7.67 75.1 50 0.38 0.02 8.88 0.07 8.65 51.7 353 0.19 54.1 6.57 15.65 0.38 0.4 0.041 0.3 3.5 40.1 4.09 1290 0.36 1.32 2.3 153.5 290 2.7 7.4 0.002 0.22 1.03 34 1 0.5 118.5 0.16 0.06 0.6 0.347 0.07 0.1 187 1.6 15.3 85 10.5J58833 UDD1510 217.798 M400-031 0.92 6.96 >10000 200 0.56 0.07 7.53 0.11 8.91 51.6 375 1.05 66.3 6.96 15.95 0.16 0.7 0.055 1.44 3.7 55.7 2.88 1510 0.48 1.02 2.2 158 290 2.8 32.3 0.006 2.57 6.18 32.6 2 0.5 115 0.14 2.24 0.6 0.347 0.25 0.2 183 930 15.4 74 20.9J58834 UDD1510 235.978 M400-032 0.1 6.1 190 30 0.25 0.01 6.34 0.08 6.2 52.1 688 0.14 5.6 7.06 13.3 0.56 0.8 0.035 0.23 2.5 43.6 8.18 1520 0.52 0.79 1.4 302 310 13.4 5.5 0.002 0.02 0.42 31.5 1 0.4 55 0.1 0.06 0.4 0.277 0.03 0.1 177 1.9 11.3 90 23.3J58835 UDD1510 239.578 M400-033 1.16 6.54 1385 30 0.22 0.06 6.4 0.12 4.23 79.5 874 0.14 193.5 6.8 13.25 0.23 0.6 0.034 0.19 1.8 35.8 3.89 1140 0.23 1.58 1.2 338 180 4.1 4.3 0.002 0.88 1.04 34.3 1 0.3 67.5 0.07 0.22 0.3 0.253 0.04 0.1 175 110 10.4 77 17.5J58836 UDD1510 249.184 M400-034 0.1 5.61 362 30 0.18 0.04 6.95 0.09 3.98 82.8 1100 0.18 26 8.4 13.65 0.44 0.6 0.039 0.07 1.7 55.1 8.39 1670 0.74 1.01 1 507 150 14.7 1.2 0.002 0.13 0.5 32.2 1 0.4 45.6 0.07 0.12 0.2 0.229 <0.02 0.1 177 22.9 10 137 14.1J58837 UDD1508 142.183 0.03 2.92 42.4 <10 0.09 0.01 4.82 0.08 1.7 89.1 1550 0.28 33.9 6.42 6.46 0.3 0.1 0.023 0.02 0.6 3 14.45 1160 0.16 0.05 0.6 1170 70 0.7 0.6 <0.002 0.08 0.44 22.5 1 0.2 48.1 <0.05 <0.05 <0.2 0.165 0.02 <0.1 114 1.4 5.2 56 2.3J58838 UDD1508 158.633 1.06 6.91 2540 70 1.01 0.18 7.68 0.1 16.25 73.7 202 0.43 320 7.77 19.3 0.24 1.5 0.058 0.25 6.8 42.6 3.75 1180 2.1 2.44 4.2 138.5 530 5.8 6.8 0.01 2.65 0.88 31.4 3 0.9 154 0.28 3.21 1.6 0.644 0.21 0.5 315 1830 22.7 109 49.8J58839 UDD1508 159.888 M400-035 0.49 7.74 221 160 0.8 0.07 7.63 0.11 19.65 43.2 213 1.44 89.4 6.47 20.8 0.14 1.7 0.071 0.93 8.2 55.9 3.19 1290 1.82 2.54 4.8 105 630 7.7 31.4 0.003 1.27 0.34 35.5 2 1.3 118.5 0.32 0.42 1.8 0.73 0.27 0.5 303 34 25.4 139 54.2J58840 UDD1508 163.090 M400-036 0.61 5.7 767 200 0.74 0.22 6.85 0.52 33.8 45.9 105 0.59 395 7.2 15.5 0.14 2 0.121 1.09 14.7 44.2 1.54 945 3.34 1.64 3.9 80.2 480 8.8 29.3 0.005 3.47 0.78 19.3 4 1.9 103 0.29 0.89 4.8 0.379 0.26 1.2 149 11.7 17.9 214 72.2J58841 UDD1508 166.298 M400-037 0.61 7.61 536 110 0.61 0.05 7.38 0.11 15.3 42.9 184 1.01 136.5 7.98 18.4 0.35 1.9 0.071 0.79 6.3 39.9 4.5 1070 0.65 1.61 3.9 99.5 670 5.6 23.5 0.002 1.02 0.48 34.8 2 1.4 152 0.26 0.35 1.4 0.67 0.28 0.4 266 85.2 20.4 128 64.1J58842 UDD1508 173.298 0.17 5.45 1085 80 0.55 0.04 13.05 0.14 13.75 48.2 327 1.1 102 6.73 14.5 0.15 0.5 0.054 0.96 5.4 38.3 2.39 1640 0.34 0.21 4.1 205 420 6.2 27.5 <0.002 0.57 0.58 25.7 1 0.7 122.5 0.24 0.21 0.6 0.608 0.3 0.1 185 8.4 15.9 87 15J58843 UDD1508 210.370 M400-038 0.07 7.06 98 20 0.22 0.02 12.45 0.07 8.71 52.2 300 0.13 114.5 6.66 14.7 0.2 0.3 0.041 0.17 3.5 27.8 3.83 1590 0.26 1.04 2.3 141.5 290 1.2 4 <0.002 0.19 1.17 32.1 1 0.5 177 0.14 0.06 0.6 0.331 0.04 0.1 168 5.7 14.9 66 6.5J58844 UDD1508 233.033 0.07 6.52 149.5 20 0.3 0.02 9.78 0.07 9.5 53.7 318 0.15 90.8 5.65 14.05 0.45 0.3 0.043 0.21 3.9 26.8 2.71 1420 0.29 1.05 2.2 143 280 1.7 4.5 <0.002 0.14 0.72 32.2 1 0.5 154 0.14 0.05 0.6 0.334 0.04 0.1 168 0.9 16.7 640 7.6J58845 UDD1508 250.093 M400-039 0.07 7.4 161.5 50 0.39 0.01 7.18 0.07 9.9 55.8 354 0.49 70.3 7.34 16 0.39 0.6 0.045 0.39 4 29.7 3.27 2090 0.29 1.35 2.4 184.5 310 1.7 9.8 <0.002 0.17 0.4 36.1 1 0.5 126 0.15 0.07 0.6 0.372 0.07 0.1 195 2.3 17.3 82 13.9J58846 UDD1508 252.051 0.08 7.81 1280 70 0.43 0.07 7.32 0.06 9.71 59.1 438 0.35 95 7.22 16 0.25 0.5 0.049 0.47 4 37 3.42 1460 0.57 1.43 2.4 190.5 310 3 10 <0.002 0.68 0.65 35.9 2 0.6 141.5 0.15 0.51 0.6 0.38 0.07 0.2 210 8.5 17.2 74 11.9J58847 UDD1508 253.117 M400-040 4.69 4.97 192.5 90 0.52 0.12 7.17 0.04 5.35 37.4 495 0.11 48.3 5.32 14.85 0.1 0.5 0.053 0.53 2.3 2.8 4.38 1340 3.92 1.15 1.3 145.5 230 3 8.1 0.003 0.31 1.08 23.1 1 0.6 108 0.08 0.76 0.3 0.202 0.09 0.1 352 371 11.3 56 12.5J58848 PERCD8151A 387.969 M400-041 0.2 6.69 647 70 0.22 0.05 9.78 0.07 4.25 114.5 965 0.14 80.5 9.31 14.05 0.34 0.5 0.042 0.42 1.7 31.3 2.01 2080 0.51 2.31 1.3 516 140 2.1 4.7 0.002 0.36 0.85 39.6 1 0.4 69.2 0.08 0.08 0.3 0.274 0.05 0.1 199 1.5 10.8 84 14.2J58849 PERCD8151A 391.759 M400-042 1.12 6.38 >10000 170 0.39 1.69 5.65 0.08 3.91 201 911 0.54 816 9.34 12.8 0.26 0.4 0.052 0.31 1.5 39.8 3.26 985 1.05 2.78 1.2 424 160 5.9 9.1 <0.002 4 20.6 35.2 3 0.4 203 0.07 1.52 0.3 0.267 0.05 0.1 195 24 10.7 58 12J58850 PERCD8151A 410.076 M400-043 0.1 2.76 675 <10 <0.05 0.05 4.57 0.04 1.8 88 1550 0.17 10.9 6.02 6.43 0.19 0.1 0.017 0.01 0.7 3.8 14.1 1250 0.13 0.03 0.5 1270 90 0.7 0.3 <0.002 0.07 1.27 20.1 1 <0.2 47.4 <0.05 0.06 <0.2 0.147 <0.02 <0.1 104 0.4 4.8 55 2.5J58851 PERCD8151A 422.669 M400-044 0.31 7.23 >10000 110 0.43 0.07 6.16 0.08 8.86 80.1 695 0.99 101.5 7.43 16.1 0.26 0.6 0.055 0.55 3.5 33.8 3.38 1670 0.32 2.52 2.3 270 280 4.1 14.9 <0.002 1.13 6.38 38.2 2 0.5 132 0.14 0.19 0.6 0.376 0.09 0.1 203 4.1 16.7 72 17.1J58852 PERCD8151A 423.494 M400-045 0.18 6.02 4720 110 0.26 0.02 6.54 0.08 3.37 90.6 1170 2.01 34.5 7.6 13.65 0.47 0.6 0.037 0.7 1.3 72.5 7.17 1640 0.32 1.07 1 532 140 2 27 <0.002 0.58 2.25 33 1 0.3 63.4 0.07 0.28 0.2 0.247 0.2 0.1 185 1 9.9 95 14.3J58853 PERCD8151A 426.499 M400-046 1.53 6.35 >10000 160 0.35 0.08 7.1 0.1 8.29 61.8 708 3.33 53.6 7.09 14.6 0.28 0.6 0.054 1.75 3.4 96.1 6.1 1760 0.48 0.95 1.9 313 250 3.1 66.6 <0.002 1.44 7.18 31.5 2 0.5 86 0.12 0.71 0.5 0.296 0.39 0.1 171 3.6 13.9 89 18.1J58854 PERCD8151A 428.911 M400-047 0.33 7.47 533 110 0.42 0.02 7.38 0.08 10.45 97.4 501 1.6 62.4 6.54 14.65 0.15 0.5 0.045 1 4.2 62.9 1.53 2170 0.42 1.68 2.7 293 330 3.4 30.7 <0.002 0.45 0.45 29.3 1 0.5 116.5 0.17 0.08 0.7 0.402 0.2 0.2 170 1.3 17 53 15.2J58855 PERCD8151A 439.504 0.28 5.54 2850 120 0.63 0.12 8.23 0.54 17.3 34 117 2.26 78.7 6.09 14.95 0.12 1.8 0.121 0.85 7.7 49.8 2.83 1110 0.7 2.32 3.8 65.8 420 8.7 27.1 0.002 1.37 2.09 22.7 2 1.7 106.5 0.28 0.19 2.8 0.476 0.3 0.9 171 7.5 17.2 273 60
A-1
3
Appendix 3: Petrographic Descriptions
A-14
Appendix 3
St Ives petrographic descriptions PTS019 Mineral abundance: quartz – 40% plagioclase – 30% hornblende – 20% carbonate – 5% biotite – 3% magnetite – 1% chlorite – 0.5% epidote – minor sericite – minor Description: Euhedral plagioclase phenocrysts up to 2mm in diamater away from the contact with mafic host rock, plus moderate sericitzation. 5:1 ratio of plagioclase to quartz phenocrysts. Quartz phenocrysts are up to 0.5mm in diameter, are subhedral, have partially dissolved grain boundaries, undulose extinction and some subgrain development. Plagioclase+quartz phenocrysts are aligned parallel to the felsic/mafic contact, and a foliation defined by needle-like hornblende. Mafic inclusions within the felsic intrusive consist of a massive chlorite background with irregularly-oriented overgrowths of elongate biotite. The mean length of the biotite long dimension is 1mm, and is aligned parallel to the main foliation. Phenocrysts are contained within a fine-grained quartz matrix. Carbonate+chlorite+quartz+epidote are contained within veins, and there is some direct replacement of plagioclase by carbonate. Magnetite porphyroblasts within the mafic portion have been partially replaced by biotite. Biotite is partially stable with hornblende, but in areas the latter was overprinted by biotite. Hornblende is also replaced by carbonate. Paragenesis: Plagioclase+quartz phenocrysts (plus igneous hornblende) deformed and aligned parallel to intrusive the contact, or possibly some magmatic alignment. Plagioclase was altered to sericite or carbonate. Mafic enclaves were altered to chlorite+biotite. Metasomatic hornblende+biotite formed a foliation and replaced primary mineralogy. Late carbonate+chlorite+quartz+sericite+epidote are within veins and are a direct replacement of higher-temp assemblages. PTS020 Mineral abundance: white mica – 45% quartz – 35% tourmaline – 10% plagioclase – 8% pyrrhotite – 2% carbonate – minor at end of thin section Description: Plagioclase clasts sub-rounded and with irregular grains boundaries, partially to strongly sericitized. Tourmaline is aligned parallel to foliation that is dominantly defined by sericite, but also has elongate pods of quartz+pyrrhotite. Tourmaline grains have a common extinction angle. Same quartz also within pull-aparts of tourmaline and plagioclase, and in veins discordant to the main foliation orientation. A white mica foliation cross-cuts plagioclase clasts. Quartz in pods and pull-aparts is up to 100µm in diameter compared to the very fine-grained matrix quartz that is intergrown with sericite. Paragenesis: Early plagioclase-phyric rock overprinted by white mica and tourmaline foliation and late-stage quartz+pyrrhotite injection/replacement of pods, veins and pull-aparts. Very minor carbonate associated with late veins/pull-aparts. PTS022
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Mineral abundance: quartz – 30% plagioclase – 30% white mica – 20% biotite – 10% chlorite – 3% carbonate – 5% magnetite – 2% pyrite – trace Description: Plagioclase-phyric average 0.5mm in diameter, partially to strongly replaced by sericite. Dominantly white mica (sericite) foliation with concentrations of muscovite within foliation-parallel aggregates that are non-continuous and contain kink-bands perpendicular to the foliation orientation. Biotite grains are weakly-aligned with the foliation, but are generally widespread throughout. Biotite within sections of the rock have undergone partial to complete retrogression to chlorite. Magnetite is disseminated throughout, but preferentially are located with biotite, possibly pseudomorphed the latter. Quartz as a fine-grained matrix. Paragenesis: Clasts were overprinted by sericite+muscovite foliation. Magnetite overprinted biotite but is stable with muscovite+carbonate. PTS110 Mineral abundance: quartz – 30% plagioclase – 30% white mica – 20% biotite – 10% carbonate – 5% magnetite – 3% rutile – 1% pyrite – 1 % chalcopyrite – trace Description: Plagioclase clasts of up to 1mm, dominantly 0.5mm, with clast perimeters deformed by a well-developed biotitie-sericite foliation, with only minor muscovite. Plagioclase is partially replaced by sericite. Magnetite is mainly confined to biotite foliations and other areas of biotite, but is also distributed through the rock. Biotite in places is partially altered to chlorite. Quartz is mainly fine-grained and in equigranular veins with carbonate. Pyrite ± chalcopyrite is disseminated throughout. Paragenesis: Plagioclase clasts deformed by biotite ± white mica foliation, with white mica more or less stable with biotite. Magnetite was replaced by biotite, the relationship to other opaques is unclear. Carbonate post-dates biotite (latter as inclusions), synchronous with quartz+carbonate veins. PTS112 Mineral abundance: quartz – 50% plagioclase – 20% biotite – 10% carbonate – 8% white mica – 6% chlorite – 4% magnetite – 2% pyrite – minor Description:
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Quartz+plagioclase phyric with most quartz contained within the groundmass. Biotite+carbonate are mainly confined to dense aggregates aligned parallel to a weak foliation. Sericite is mainly a replacement of plagioclase clast rims and as sauseritization. Quartz clasts are also deformed/truncated when in contact with fine-grained quartz+sericite zones. Carbonate grains overgrew twinning in plagioclase. Chlorite partially to completely replaced biotite. Paragenesis: Plagioclase+quartz clasts were deformed and replaced by the fine-grained quartz+sericite+carbonate foliation. Biotite was replaced replaced by chlorite+carbonate and the former may have been the product of a mafic clast/precursor. PTS113 Mineral abundance: hornblende – 45% biotite – 25% quartz – 25% chlorite – 2% pyrrhotite – 2% magnetite – 1% titanite – minor chalcopyrite – minor Description: Elongate, bladed, hornblende-rich rock, intergrown with biotite. Titanite is mainly associated with biotite-rich zones. Interstitial fine-grained quartz – no recognizable plagioclase – but coarser where associated with chlorite, pyrrhotite and chalcopyrite. Magnetite – at times skeletal – with dissolution texture within framework of hornblende+biotite+pyrrhotite+chalcopyrite is mainly resticted to quartz+chlorite-bearing veins. Paragenesis: Within variolitic Paringa Basalt. Biotite-rich zones delineate variole edges, and creates an overall concentric pattern. Chlorite+quartz+pyrrhotite+chalcopyrite in veins is a product of late-stage alteration; chlorite after biotite+hornblende. Magnetite is not in equilibrium with, and pre-dates hornblende+biotite. PTS002 Mineral abundance: plagioclase – 50% biotite – 30% quartz – 8% pyrite – 8% pyrrhotite – 2% chlorite – 1% carbonate – 1% sphalerite – minor chalcopyrite – minor magnetite – minor monazite – trace Description: Most of the rock is comprised of equigranular, subrounded, ~50 µm-sized plagioclase grains with interstitial biotite crudely arranged into a weak foliation, or series of multiply-oriented/short strike-length fabrics. Spaced sets of relatively coarse plagioclase are arranged as tension veins with long axes parallel to the weak biotite foliation. Pyrrhotite+chalcopyrite+sphalerite is solely situated within the tension veins, where it is in equilibrium with plagioclase and biotite. Concentrations of biotite envelop the veins, and contain rare monazite? Chlorite overprinted biotite in proximity of the most well-developed foliation in the thin section, and is in equilibrium with, and spatially associated with carbonate (after plagioclase), quartz and large subhedral pyrite grains. Pyrite grains contain inclusions of intergrown pyrrhotite+chalcopyrite+sphalerite, whereas sphalerite within the pyrrhotite domain has pyrrhotite+chalcopyrite inclusions. Minor magnetite grains with ragged rims are restricted to a narrow
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interval between the chlorite+pyrite domain and plagioclase+pyrrhotite-bearing tension veins, and were partially replaced by biotite. Quartz is predominantly restricted to areas of greatest pyrite concentration, and is a spotty overprint on plagioclase. Paragenesis: Early euhedral magnetite was replaced by biotite. Plagioclase+biotite+pyrrhotite+sphalerite+chalcopyrite-filled veins were overprinted by quartz+carbonate+chlorite+pyrite. Biotite was partially stable with pyrite growth but retrogressed in zones of greatest fluid infiltration. PTS016 Mineral abundance: chlorite – 50% carbonate – 20% biotite – 15% quartz – 10% magnetite – 5% tourmaline – minor zircon – minor Description: Chlorite foliation after actinolite? deformed and fractured earlier plagioclase grains of up to 3 mm in diameter. Carbonate and lesser quartz further replaced plagioclase. Disseminated biotite grains of an average 0.5 mm diameter overgrew the chlorite foliation and is pre-syn carbonate. Zircon is locally abundant within biotite. Carbonate+magnetite±quartz±tourmaline-bearing veins have some infill/selvage of relict chloritized amphibole/actinolite at vein margins. Tourmaline overgrew biotite grain boundaries. Paragenesis: Plagioclase clasts within mafic/silt unit of the Black Flag Beds were deformed and replaced by an initially amphibole?, then chlorite foliation. Biotite porphs overgrew the chlorite foliation and were still in equilibrium with carbonate+magnetite±quartz±tourmaline-bearing veins, but overprinted the latter. PTS017 Mineral abundance: hornblende – 50% plagioclase – 20% chlorite – 15% quartz – 9% magnetite – 3% carbonate – 3% epidote – minor biotite – minor pyrite – minor/trace Description: 3-4 mm diameter, partially- to strongly-altered plagioclase grains were fractured and replaced by fine-grained quartz+plagioclase? and acicular hornblende. Hornblende can also be coarse lathes, to fine-grained aggregates that cover most of the thin section. Veins cross-cut large plagioclase grains, and contain carbonate, quartz (and fine-grained plagioclase?) and needles of hornblende oriented perpendicular to vein walls. Veins extend from foliation zones that are defined by chlorite (after hornblende), quartz, magnetite and intergrown euhedral epidote grains. A few grains of hornblende appear to overprint the chlorite-altered foliation, but on the whole across the thin section, rims of hornblende grains were partially altered to chlorite. Minor biotite is intergrown with chlorite as a replacement of hornblende. Magnetite formed irregular grains intergrown with quartz (symplectic) and chlorite). Paragenesis:
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Plagioclase phenocrysts in dolerite were fractured and replaced by hornblende+quartz+secondary plagioclase? Later alteration was focussed within foliation zones in the form of chloritization and minor biotization of hornblende; and carbonate reflected the same fluid phase in the last stage of veining. Magnetite, quartz, carbonate, epidote, chlorite and biotite replaced hornblende+secondary plagioclase?+quartz. PTS026 Mineral abundance: quartz – 50% carbonate – 25% sericite – 10% biotite – 10% pyrite – 5% pyrrhotite/chalcopyrite – minor Description: Relict layering is defined by varying proportions of quartz, carbonate and biotite. Carbonate as small irregularly-shaped grains intergrown with biotite within a fine-grained quartz matrix, and as relatively large 1 mm-sized grains with layering-parallel and layering discordant quartz-carbonate veins. Concentrations of biotite and muscovite define foliations both parallel and discordant to quartz+carbonate veins, and is most dense where the latter is off-set and folded by the foliation. Minor pyrrhotite/chalcopyrite rim pyrite adjacent to the biotite+muscovite foliation. Paragenesis: Quartz+plagioclase layered rock deformed by biotite+muscovite foliation that was synchronous with quartz+carbonate vein growth. PTS028 Mineral abundance: quartz – 35% plagioclase – 20% chlorite – 20% carbonate – 15% magnetite – 3% biotite – 2% pyrrhotite – minor chalcopyrite – minor monazite? – trace Description: Partially to completely sericitized/carbonatized plagioclase grains have fracture-infill and are enveloped by a chlorite foliation after early actinolite? Coarse hornblende is syn-post chlorite that defines the main foliation; ie. sometimes parallel to the foliation, with the latter partially wrapping around hornblende, but is also a static overgrowth. Biotite partially overgrew the chlorite foliation and is also associated with quartz within euhedral magnetite strain shadows. Quartz+carbonate-filled veins are parallel and oblique to the main foliation. Hornblende and biotite are spatially associated with and in equilibrium with pyrrhotite+chalcopyrite. Minor monazite within chlorite foliation? Paragenesis: Igneous/metamorphic plagioclase was deformed by an actinolite? foliation that was replaced by chlorite. Hornblende+biotite+pyrrhotite+chalcopyrite was pre-syn the introduction of magnetite porphyroblasts+quartz+biotite and quartz+carbonate-filled veins. Refer also to PTS016. PTS114 Mineral abundance: hornblende – 40% plagioclase – 30% quartz – 15% chlorite – 7 % biotite – 2%
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carbonate – 2% pyrrhotite – 2% prehnite – 1% sericite – 1% Description: Acicular hornblende intergrown with medium to fine-grained plagioclase and quartz. Hornblende was replaced by Mg-chlorite? with proximity to cm-scale plagioclase+quartz+pyrrhotite-filled vein, and plagioclase within the vein and matrix was replaced by sericite and carbonate. Pyrrhotite is spatially associated with quartz, carbonate, prehnite and chlorite, and is mainly distributed within the plagioclase vein. prehnite in particular forms narrow rims around the sulphide grains. Biotite is intergrown with hornblende. Paragenesis: Hornblende+plagioclase+biotite were replaced by chlorite+carbonate+prehnite +quartz+pyrrhotite. PTS121 Mineral abundance: quartz – 30% carbonate – 20% sericite – 15% muscovite – 11% biotite – 10% chlorite – 5% tourmaline – 5% pyrrhotite – 4% sphalerite – minor Description: background of very fine-grained plagioclase+quartz+sericite with larger disseminated biotite grains and dispersed, intergrown tourmaline. Coarse (up to 250 µm) quartz+carbonate+partially chloritized biotite+chlorite+muscovite+pyrrhotite± sphalerite within veins cross-cut the formerly textured rock. Tourmaline is in equilibrium with the vein assemblage. Muscovite+biotite also form localized foliations within the vein domain. Paragensis: Fine-grained quartz+plagioclase+sericite and disseminated biotite+tourmaline was overprinted by a coarser assemblage of quartz+muscovite+chlorite+carbonate+pyrrohtite±sphalerite. PTS122 Mineral abundance: hornblende – 50% chlorite – 30% carbonate – 10% biotite – 5% pyrite – 3% magnetite – 2% Description: Coarse hornblende grains up to 2 mm long are intergrown and are predominantly aligned parallel to a well-defined biotite foliation. Hornblende grains at a discordant angle to the biotite foliation appear to statically overprint the latter. Intergrown chlorite+carbonate+magnetite+pyrite is most well developed at one end of the thin section. Chlorite preferentially replaced biotite in all except one end of the thin section, and carbonate+fine-grained disseminated magnetite partially replaced hornblende, although the latter was much more stable than biotite, and well-preserved within the intensely-developed carbonate-chlorite zone. 1-2 mm-sized euhedral pyrite statically overprinted early hornblende+biotite. Paragenesis: Hornblende+biotite was replaced by a chlorite+carbonate+magnetite+pyrite assemblage.
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PTS123 Mineral abundance: biotite – 40% carbonate – 30% quartz – 15% hornblende – 10% plagioclase – 5% Description: Relict plagioclase clasts within a biotite foliation are mostly replaced by carbonate, and are at best partially altered. Coarse hornblende up to 3 mm-long are mainly oriented subparallel to the biotite foliation, but are also commonly oriented at more than 45° to the foliation plane. Carbonate+quartz+pyrite partially replaced hornblende+biotite and is concentrated in layers parallel to the biotite foliation. Paragenesis: Plagioclase phenocrysts in dolerite are in equilibrium with the biotite+hornblende foliation. Carbonate+quartz+pyrite replaced the earlier mineral assemblage. M400-117 Mineral abundance: carbonate – 40% chlorite – 30% quartz – 10% white mica – 10% pyrite – 7% rutile – 3% Description: Intense chlorite±white mica foliation is cross-cut by carbonate-bearing veins. Carbonate that overprinted the foliation preserve the habit of relict hornblende grains Chlorite and white mica is stable with carbonate and pyrite. Paragenesis: An early foliation was overprinted by hornblende, but textures are unable to differentiate whether all chlorite is related to late carbonate replacement/veining or chlorite was the original foliation-defining mineral. M400-118 Mineral abundance: chlorite – 40% plagioclase – 20% carbonate – 20% quartz – 15% biotite – 2% rutile/ilmenite – 2% pyrite – 1% Description: Weak foliation in host rock defined by chlorite. The main vein that cross-cuts the foliation contains massive, fine-grained chlorite and coarse-grained albite lathes mainly confined to vein margins. Carbonate instead of plagioclase dominate the centre of the vein, but relict grain shapes are indicative of plagioclase. Fine-grained albite+quartz occupy the selvage to the vein, but also extend into domains that intervene the foliated chlorite layers. Lesser biotite is restricted to the proximal vein selvage. Pyrite mainly occupies quartz+carbonate veins, and rutile/ilmenite is hosted by chlorite and carbonate. Paragenesis: Albite+chlorite? veins overprinted foliated matrix of unknown mineral precursor. Chlorite+carbonate is partially stable with biotite+plagioclase although the former replaced the latter. Carbonate+chlorite+quartz+rutile are co-stable as the latest assemblage.
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M400-119 Mineral abundance: chlorite – 30% carbonate – 20% quartz – 20% biotite – 15% actinolite – 5% clinozoisite – 5% rutile - 5% titanite – minor Description: Massive actinolite host overprinted by circular aggregates of chlorite+biotite+quartz (same as in TD10269 – M400-133). Actinolitic host was cross-cut by a foliation that is defined by mineral domains that comprise chlorite+quartz+biotite+carbonate +clinozoisite. Chlorite+biotite+carbonate+clinozoisite overgrow a relict mineral cleavage - similar to actinolitic habit of host – within lithons between foliation planes. Biotite formed as stubby grains that consistently have chlorite rims. Stubby carbonate grains similarly overprint predominantly chlorite-altered precursor, and extend into the chlorite+quartz foliations beyond. Fine-grained clinozoisite is restricted to the chlorite+biotite+carbonate-altered precursor. Angular, subhedral titanite is restricted to a particular horizon. Rutile is predominantly associated with chlorite. Paragenesis: Actinolite+titanite host was deformed and altered by chlorite+biotite+carbonate+clinozoisite+rutile. M400-120 Mineral abundance: chlorite – 40% quartz – 30% carbonate – 10% actinolite – 10% rutile – 7% biotite – 2% clinozoisite – 1% Description: Host contains massive actinolite partially altered to chlorite, and with cores overgrown by a collection of elongate clinozoisite grains arranged within hexagonal prisms. Actinolite grains are slightly elongate and have strongly developed internal cleavage. There is some internal subgrain development within the actinolite. Amygdales and veins are zoned with secondary actinolite+chlorite+biotite+carbonate+quartz. The veins bisect primary actinolite grains within the host. Rutile is concentrated at primary actinolite margins and within selvage to veins. Paragenesis: Metamorphic actinolite was partially-altered to hornblende within grain cores. During vein/amygdale development, the hornblende was altered to clinozoisite±chlorite, whereas actinolite was cross-cut and replaced by secondary actinolite+chlorite+carbonate+quartz+biotite+rutile. Textures are indicative of mineral precipitation under epithermal conditions. M400-121 Mineral abundance: chlorite – 40% quartz – 15% biotite – 15% carbonate – 15% rutile – 10% tourmaline – 5% Description:
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Chlorite defines the penetrative fabric, with some evidence of pre-existing amphibole grain shapes and cleavage. Strange texture involving interlayered rutile and quartz that is discordant to the penetrative fabric, but is confined by spaced foliation planes. Biotite is intergrown with the rutile+quartz layering, and coarse-grained porphyroblasts also overgrew the penetrative fabric. Tourmaline overprinted biotite cleavage and grain margins. Quartz+carbonate domains are both parallel to and discordant to the penetrative fabric, and contain partially replaced tourmaline. Tourmaline is devoid from quartz+rutile-layered domains. Paragenesis: An early amphibole-rich rock was replaced/foliated by chlorite and syn-post development of layered rutile+quartz+biotite within selected domains. Tourmaline replaced biotite+chlorite within quartz+rutile-free domains, and was replaced by carbonate+quartz during the last alteration event. M400-122 Mineral abundance: chlorite – 32% biotite – 25% carbonate – 15% quartz – 10% tourmaline – 8% clinozoisite – 6% pyrite – 4% Description: Chlorite within foliations and as selvage to aggregates of mainly biotite+carbonate+quartz+pyrite. There is direct replacement of amphibole by clinozoisite within biotite-dominated zones, but within the clinozoisite+chlorite selvage to the former domains, clinozoisite grains approach a diagnostic columnar habit. Tourmaline and clinozoisite predominantly developed within disparate domains, but there is some overlap where the two are intergrown (photomicrograph - M400_122_Trans/XPol1). Tourmaline+clinozoisite both overgrew biotite grain margins and were both partially to completely replaced by carbonate where grains overlap with carbonate+quartz zones. Paragenesis: Amphibole was completely replaced by chlorite+biotite±tourmaline±clinozoisite, but tourmaline+clinozoisite formed syn-post biotite. Biotite was stable through-out late carbonate+quartz+pyrite alteration, where tourmaline+clinozoisite were mainly replaced by carbonate. M400-123 Mineral abundance: carbonate – 30% chlorite – 30% quartz – 20% biotite – 15% Pyrrhotite/pyrite – 5% plagioclase - minor Description: Lenses of relict plagioclase have been overprinted by chlorite+carbonate+biotite. A chlorite+quartz±biotite foliation envelops the lenses. Biotite was partially replaced by chlorite. Pyrite rims pyrrhotite. Pyrrhotite/pyrite overgrew biotite lathes and is intergrown with carbonate+quartz. Paragenesis: Plagioclase+amphibole? porphyroblasts were deformed during alteration to chlorite+biotite. Ensuing carbonate+quartz+pyrrhotite/pyrite alteration resulted in the partial replacement of biotite to chlorite and continuing alteration of plagioclase+amphibole to carbonate+chlorite. M400-124 Mineral abundance: quartz – 35% biotite – 30%
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carbonate – 10% chlorite – 10% amphibole – 7% rutile – 6% clinozoisite – 1% magnetite – 1% pyrite – minor Description: A vein containing amphibole+carbonate+quartz+chlorite has its margin concordant with the main foliation. The main chlorite+quartz foliation is throughout the host rock and parts of vein, but is most well-developed at the vein margin. In parts, amphibole defines a foliation – including and S-C fabric – and was partially replaced by carbonate. Finely-disseminated magnetite is confined to the vein selvage. Clinozoisite grains with hexagonal shape are preserved within a narrow selvage layer most proximal to the vein, but sparsely disseminated grains throughout the host rock – sometimes associated with minor quartz veining – have been strongly altered to rutile. Rutile is also associated with quartz veins. Biotite is disseminated throughout the host rock, and was altered to chlorite with vicinity to the vein. Paragenesis: Amphibole within the vein was possibly co-stable with biotite within the host. Chlorite+clinozoisite replaced biotite+amphibole, and clinozoisite was altered to rutile during latest chlorite+quartz+carbonate+rutile alteration. M400-125 Mineral abundance: albite – 30% chlorite – 20% carbonate – 20% biotite – 15% quartz – 10% plagioclase (matrix) – 3% pyrrhotite: 2% pyrite – minor Description: Massive biotite and plagioclase matrix, with carbonate and chlorite overprinting grain boundaries of the former. Albite-bearing veins also contain quartz, carbonate, chlorite, biotite, pyrrhotite, and lesser pyrite. Biotite, chlorite and carbonate are co-stable within the vein. Carbonate, chlorite, biotite and quartz form within mono-mineralic domains that overprinted albite grain boundaries. In some cases, chlorite partially altered albite in the form of small, disseminated grains. Narrow layers of quartz±biotite separate albite at grain boundaries. Pyrrhotite is rimmed by minor pyrite. Paragenesis: Early host (including primary plagioclase?) cross-cut by albite veins with biotite selvage. Carbonate+chlorite+biotite+quartz+pyrrhotite+pyrite are a late, static overprint. M400-126 Mineral abundance: albite – 30% chlorite – 30% carbonate – 30% biotite – 5% pyrite – 5% K’spar – minor Description: Plagioclase in matrix with overprinting carbonate and quartz. Chlorite foliations with disseminated biotite. Albite-filled vein with biotite selvage partially altered to chlorite. Fracture network infilled by
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quartz+carbonate+chlorite+biotite+K’spar? +albite? Green biotite at perimeter of vein is closely associated with sulphide. Pyrite+biotite preserve relict magnetite grain shapes. Paragenesis: Early plagioclase – including albite within the vein - was fractured and infilled/overprinted by quartz+carbonate+chlorite+biotite+sulphide+K’spar? Biotite selvage to the vein was altered to chlorite as well as a green biotite. M400-129 Mineral abundance: plagioclase – 40% biotite – 20% chlorite – 15% quartz – 10% carbonate – 8% magnetite – 5% tourmaline – 2% Description: Needle-like chlorite grains radiate out from euhedral plagioclase grains suspended in fine-grained plagioclase+quartz groundmass. Plagioclase is weakly seritized/carbonatized. Most chlorite defines a weak, mainly non-continuous foliation that was statically overgrown by stubby biotite porphyroblasts. Biotite+plagioclase+quartz also occupy veins that are coeval with disseminated biotite growth. Tourmaline overprints biotite grain boundaries. Veins also contain carbonate+magnetite and particularly coarse-grained chlorite compared to the matrix-hosted phase. Biotite is particularly prone to carbonate+magnetite alteration. Paragenesis: A volcaniclastic rock comprised of plagioclase clasts within a groundmass of varying composition had a chlorite foliation develop when deformed. Later deformation resulted in biotite+plagioclase veins and syn-post tourmaline that were retrogressed to carbonate+magnetite+chlorite. M400-130 Mineral abundance: actinolite – 40% chlorite – 15% quartz – 10% clinozoisite-epidote – 10% carbonate – 8% biotite – 8% plagioclase – 5% ilmenite – 4% pyrite – minor rutile – minor Description: Fibrous, twinned actinolite as the main matrix mineral. Cross-cutting, folded vein comprising zoned feldspar, chlorite, quartz, carbonate and clinozoisite-epidote. Feldspar contains myrmekite texture similar to specimens that contain intergrown albite+orthoclase. Single grains of clinozoisite-epidote contain compositionally-zoned cores of clinozoisite and rims of epidote. Clinozoisite is typically intergrown with chlorite, whereas epidote is intergrown with quartz+carbonate. Clinozoisite replaced actinolite at vein margins, evidenced by relict twinning preserved within the former. Stubby grains of disseminated biotite are in equilibrium with a network of carbonate+quartz-filled veins that cross-cut the matrix, and are also coeval with clinozoisite-epidote and an intense chlorite foliation at one end of the thin section. Minor pyrite is contained within the large vein, and prismatic ilmenite that overgrew actinolite is contained within the matrix and chlorite foliation. Paragenesis: Actinolite was altered by biotite, ilmenite, carbonate, quartz, clinozoisite-epidote, feldspar and chlorite.
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M400-131 Mineral abundance: carbonate – 30% plagioclase – 25% chlorite – 20% quartz – 10% biotite – 7% pyrrhotite – 5% tourmaline – 3% Description: Chlorite forms an intense, dominant fabric that also contains disseminated tourmaline confined to certain foliation planes. The dominant fabric is cross-cut/folded by a crenulation predominantly defined by chlorite. Coarse plagioclase and biotite overgrew the dominant foliation and the long axes of grains are oriented parallel and are partially intergrown with chlorite crenulation, although chlorite partially replaced biotite. Fine-grained quartz and carbonate overprinted plagioclase, and pyrrhotite cross-cut biotite+plagioclase+tourmaline, but is costable with chlorite+quartz+carbonate. Paragenesis: Early foliation/layering was altered/cross-cut by biotite+plagioclase+tourmaline, which was then replaced by chlorite+quartz+carbonate+pyrrhotite. M400-132 Mineral abundance: actinolite-tremolite – 50% quartz – 35% chlorite – 9% carbonate – 5% clinozoisite – 1% biotite – minor rutile – minor Description: Fibrous actinolite matrix with cross cutting quartz+carbonate veins. Selvage to veins (including internally) is comprised of chlorite, fibrous tremolite and lesser clinozoisite. Chlorite+tremolite+clinozoisite are intergrown. Minor biotite is co-stable with chlorite and carbonate in small-scale veins within the actinolite matrix. Rutile is disseminated throughout the matrix. Paragenesis: Actinolite was overprinted and replaced by chlorite, quartz, carbonate, tremolite, clinozoisite and biotite within veins, and rutile+chlorite as a direct replacement. M400-133 Mineral abundance: TD10269 actinolite – 50% chlorite – 30% biotite – 10% rutile – 5% plagioclase – 3% quartz – 2% carbonate – minor magnetite - minor TD10465 chlorite – 40% hornblende – 20% carbonate – 20% quartz – 15% rutile – 3% pyrite – 2%
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Description: TD10269 – Radial aggregates of actinolite with edges altered to chlorite. Plagioclase+quartz form elongate, bladed grains. Biotite aggregates are associated with quartz and chlorite at margins. TD10465 – Chlorite-foliated rock overprinted by hornblende grains. Carbonate+quartz+rutile+pyrite replaced hornblende. Paragenesis: TD10269 – Metamorphic actinolite+plagioclase preserved original bladed texture of Mg-rich protolith. Biotite+chlorite+rutile+quartz replaced actinolite+quartz. TD10465 – Hydrothermal hornblende statically overprinted chlorite-foliated rock. M400-134 Mineral abundance: TD10269 144-145 m: chlorite – 40%, actinolite – 30%, carbonate – 10%, biotite – 10%, rutile – 5%, quartz – 3%, plagioclase – 2% 138-139 m: carbonate – 40%, chlorite – 20%, quartz – 20%, rutile – 10%, biotite – 8%, titanite – 2% 129-130 m: chlorite – 40%, carbonate – 20%, quartz – 20%, rutile – 20% TD10465 chlorite – 30%, carbonate – 20%, quartz – 20%, rutile, 18%, hornblende – 6%, biotite – 4%, pyrite – 2% Description: TD10269 – heterogeneously-distributed domains of chlorite, carbonate, rutile and quartz with biotite disseminated throughout. Relict actinolite preserved yet overprinted by other mineral phases within 144-145 m. TD10465 – Very similar mineral assemblage/textures to TD10269 129-130 m, but static overgrowth of hornblende+biotite upon chlorite foliation. Lower percentage hornblende at TD10465 154-155 m than in 150-151 m due to greater replacement by carbonate+rutile+quartz in former. Paragenesis: As in M400-133.
Plutonic petrographic descriptions
M400-010 Mineral abundance: biotite – 60% amphibole – 25% quartz – 10% chlorite – 5% pyrite – minor magnetite – minor rutile – minor Description: Biotite defines a foliation on one plane, which is intersected by innumerable veins of biotite, neither of which transgresses the other. Groundmass amphibole (100 µm-long needles, common radial habit) show signs of partial replacement to biotite, but definitely underwent partial to complete alteration to chlorite+ilmenite/rutile. Quartz occurs within the groundmass and also in minor accumulations of up to 100 µm-sized grains that have undulose extinction to sub-grain boundaries and irregular grain boundaries. one end of the section is dominated by coarse intergrown amphibole+biotite, of up to 0.5 mm in length. Pyrite/arsenopyrite? is rimmed by magnetite/ilmenite and statically overprint silicate assemblages, but neither show any sign of associated alteration of the latter. Paragenesis: Early amphibole+quartz alteration of ultramafic rock is locally intergrown with coarse biotite. Biotite within veins and foliations are syn-post amphibole. Chlorite and sulphide post-date amphibole+biotite, but cannot be paragentically linked.
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M400-011 Mineral abundance: actinolite – 70% tourmaline – 15% tremolite – 5% talc – 5% calcite – 5% magnetite/ilmenite/pyrite – minor rutile – minor Description: Tourmaline grains >1 mm in diameter in sections perpendicular to the c-axis, aligned within a deformed/folded plane that is also occupied by actinolite+tremolite+talc+calcite. Most of the thin section comprises a very fine grained actinolite foliation that wraps around and partially cross-cuts the tourmaline layer. Actinolite replaced tourmaline including inclusions of the former within the latter that are in alignment with the actinolite-defined foliation. Tremolite+talc+calcite predominantly occupy tourmaline pull-aparts and veins that cross-cut and replace the actinolite foliation. Micron-scale sub-rounded clasts/porphyroblasts of tremolite+talc are hosted by the actinolite foliation. Skeletal to irregular grains of magnetite? with ilmenite/pyrite inclusions are spatially associated with tremolite+calcite+talc veins. Rutile spotting transgresses broad, foliation-parallel zones of actinolite. Paragenesis: Tourmaline is the arlies-recognized mineral, and was overprinted/replaced by actinolite. Tremolite+talc+calcite+ilmenite/magnetite/pyrite replaced actinolite and cross-cut tourmaline and actinolite within pull-aparts and veins. Rutile is possibly related to the formation of the other opaques. M400-012 Mineral abundance: chlorite – 30% amphibole – 25% calcite – 25% quartz – 18% biotite – 3% magnetite/ilmenite/rutile – 2% clinozoisite – 1% pyrrhotite – 1% arsenopyrite – minor titanite – minor plagioclase – trace gold – trace chalcopyrite – trace sphalerite – trace Description: Amphibole- and quartz-layered/foliated rock, with the former partially altered to chlorite. Biotite and fine grained rutile? are restricted to certain foliation planes, and partially replaced amphibole. Biotite also partially altered to chlorite. Fine-grained quartz has undulose extinction. Calcite with lobate grain boundaries is hosted within veins with minor sub-rounded grains of clinozoisite+quartz±plagioclase. Calcite veins are parallel to and at a high angle to the foliation. The most intense zones of clinozoisite are associated with chlorite. Titanite is predominantly restricted to discrete layers. Magnetite+ilmenite/rutile is parallel to the foliation, with ilmenite as inclusions in magnetite (similar to M400-011). There is also some cross-cutting sulphide upon magnetite/ilmenite. Pyrrhotite+chalcopyrite+sphalerite rim arsenopyrite grains. There is visible gold within amphibole adjacent to pyrrhotite, and within pyrrhotite or chalcopyrite. Most sulphide is adjacent to or rim calcite veins. Paragenesis:
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Amphibole+biotite+titanite was replaced by chlorite+calcite+clinozoisite. Ilmenite/magnetite/rutile (except for rutile needles in biotite) are associated with chlorite+calcite+clinozoisite; and arsenopyrite was first in a sequence of sulphide growth that was coeval with veining. M400-013 Mineral Abundance: amphibole – 60% chlorite – 25% biotite – 4% carbonate – 3% rutile – 3% pyrrhotite – minor plagioclase – minor titanite – minor Description: Amphibole (hornblende) occurs as massive growths and within concentric aggregates (1 cm diameter), and is intergrown with biotite+tourmaline in foliations and veins. Chlorite is a replacement of hornblende and biotite, and is associated with an accumulation of rutile. Also, needle-like rutile is intergrown with biotite. Quartz is interstitial to amphibole+biotite, especially in veins. Carbonate statically replaced amphibole and is common to veins comprised of pure carbonate. Pyrrhotite is predominantly contained within biotite+amphibole foliations and is rimmed by rutile. Titanite is intergrown with hornblende on aggregate margins. Plagioclase with albite twins is intergrown with chlorite after hornblende. There is partial replacement of plagioclase to carbonate. Paragenesis: Amphibole+plagioclase+titanite was replaced by chlorite+biotite+carbonate+rutile. The timing of pyrrhotite is unknown. M400-014 Mineral abundance: chlorite – 60% amphibole – 35% rutile – 2% biotite – 2% carbonate – 1% pyrrhotite – minor tourmaline – trace quartz – trace Description: Chlorite+biotite replaced amphibole within foliated zones; amphibole preserved as elongate clasts/aggregates. Carbonate spotting and rutile are confined to chlorite+biotite zones. Pyrrhotite is rimmed by rutile. Talc or tremolite partially replaced amphibole rims. Paragenesis: Amphibole+tourmaline+quartz was replaced by chlorite+biotite+carbonate+rutile +pyrrhotite. Rutile was syn-post pyrrhotite. M400-015 Mineral abundance: chlorite – 40% talc – 30% tremolite – 10% carbonate – 10% magnetite – 9% rutile – 1% Description:
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Veins comprised predominantly of chlorite, carbonate or talc+tremolite, are surrounded by a foliated matrix of alternating chlorite and talc zones with disseminated magnetite. The matrix partially preserves relict spinifex texture. Paragenesis: All minerals appear to be in equilibrium; ie. veining is coincident with the complete replacement of pre-existing minerals within matrix as contained within the former. M400-016 Mineral abundance: talc – 45% chlorite – 24% tremolite – 15% magnetite – 9% carbonate – 5% serpentine – 1% Description: Talc is intergrown with chlorite and magnetite in a fine-grained, generally massive matrix; with minor relict spinifex texture particularly preserved adjacent to relict olivine grains. Clasts (relict olivine) with one long dimension are up to 0.5 cm in length and have chlorite-dominant cores that preserve a relict asbestiform habit. Chlorite cores are rimmed by carbonate and an outermost concentration of magnetite; which is relatively coarse compared to matrix-hosted magnetite. Chlorite or talc is also contained within veins that are intergrown with partially-replaced serpentine and have a magnetite selvage. Rare, 1 cm-sized carbonate grains are contained at one end of the thin section. Minor pyrite and trace chalcopyrite are within the matrix and at the rims of chlorite/carbonate clasts. There is a well-formed chlorite+talc foliation within parts of the thin section. Paragenesis: A matrix-supported olivine cumulate had at least the coarser fraction altered to serpentine, and then was partially- to completely-converted to chlorite+talc+carbonate+magnetite. Relict olivine/serpentine grains were deformed and aligned // to the foliation. M400-017 Mineral abundance: chlorite – 60% talc – 20% serpentine – 9% tremolite – 5% carbonate – 3% magnetite – 3% pyrite/pyrrhotite/chalcopyrite – minor Description: Pyrite/pyrrhotite/chalcopyrite are rimmed by magnetite. Half cm- to 1 cm-diameter, partially chlorite-altered serpentine clasts are within medium-grained cumulate-textured matrix of chlorite and lesser talc. Minor second-order birefringence outlines relict ?olivine?. Magnetite is concentrated along cleavage planes of relict olivine and within foliation planes and veins that are defined by chlorite and talc, and carbonate and partially-replaced serpentine, respectively. One end of the thin section is dominantly massive talc-carbonate. Couldn’t recognize pyrophyllite; very hard to distinguish talc from white mica/pyrophyllite. Paragenesis: Crystal-rich olivine cumulate with partially-preserved serpentine that replaced the largest of the olivine phenocrysts. Serpentine-filled veins represent the first deformation/alteration event followed by chlorite-talc-carbonate-magnetite that delineated the same structures. Unknown origin of sulphide, but overprinted by a late magnetite phase? M400-018 Mineral abundance:
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talc – 40% chlorite – 40% tremolite – 10% carbonate – 5% serpentine – 5% pyrite/chalcopyrite – minor rutile/ilmenite/magnetite? – minor Description: Equigranular talc-chlorite rock with stubby grains of talc and interstitial chlorite. Partially chloritized serpentine-bearing veins and carbonate-bearing veins mutually cross-cut. Serpentine has asbestiform texture and unusual 2nd order birefringence colours (up to blue) that decrease with increasing chlorite replacement (similar to M400-017). Rutile is associated with minor ilmenite within chlorite that is in equal proportions to the amount of pyrite and chalcopyrite. Paragenesis: Serpentine-carbonate veins cross-cut rock that was homogeneously altered to talc-chlorite. M400-019 Mineral abundance: chlorite – 45% talc – 40% carbonate – 10% tremolite – 5% pyrite/pyrrhotite/chalcopyrite/magnetite? – minor Description: Approximately half of thin section contains very fine-grained talc+chlorite, and the other half coarse-grained chlorite+talc within veins. Bladed, to radial amphibole – tremolite? – distribution was replaced by chlorite & talc. Pyrite?+pyrrhotite+sphalerite (no internal refelction but a darker colour than magnetite) +chalcopyrite is intergrown at vein margins. Magnetite is associated with chlorite but not with sulphide. Paragenesis: Veins initially formed and filled with amphibole, then were replaced during later chlorite+talc+sulphide? event. M400-020 Mineral abundance: quartz – 40% hornblende – 23% carbonate – 20% chlorite – 5% garnet – 4% magnetite/ilmenite – 3% amphibole – 2% biotite – 2% pyrrhotite/chalcopyrite/sphalerite – 1% zircon – minor Description: Two main zones: hornblende+fine-grained interstitial quartz+biotite and minor zircon within former, and medium-grained (100-500µm) carbonate+quartz. Carbonate in the second zone is associated with chlorite that replaced hornblende. Chlorite is confined to foliations. Carbonate veins cross-cut hornblende. Some evidence of two generations of hornblende? minor phase (amphibole) forms needle-like foliations zones. Garnet is situated throughout both zones and is in equilibrium with both phases of hornblende but was replaced by chlorite+carbonate. Hornblende+garnet have inclusions of magnetite/ilmenite that are also concentrated within chlorite. Biotite+amphibole foliation was overprinted by chlorite+ilmenite? at one end of the thin section. Alignment of hornblende+garnet is at approximately 30° to the chlorite-defined foliation and the contact between the former and the
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carbonate+quartz zone. Pyrrhotite+chalcopyrite+sphalerite is predominantly at the perimeter of chlorite+carbonate foliations/veins and a small percentage as a replacement of garnet. Paragenesis: Hornblende grains are pre-syn development of amphibole+biotite foliations, but syn garnet+zircon growth. chlorite+carbonate replacement/veins are post hornblende+biotite+garnet and syn ilmenite/magnetite?+pyrrhotite+chalcopyrite+sphalerite. M400-021 Mineral abundance: actinolite – 80% carbonate – 10% Feldspar – 10% pyrrhotite/chalcopyrite/sphalerite – trace prehnite - trace Description: Fine-grained actinolite defines a foliation, with intervening, irregularly-distributed grains and interstitial fine-grained feldspar and carbonate. A few areas of massive actinolite. Cross-cutting feldspar+carbonate veins with rare prehnite. Trace Po+Cpy+Sph with feldspar veins. Paragenesis: Actinolite as a metamorphic phase was overprinted/replaced by feldspar/carbonate/sulphide. M400-022 Mineral abundance: carbonate – 40% quartz – 30% clinozoisite – 20% hornblende – 9% titanite – 1% pyrrhotite – minor pyrite – trace serpentine – trace? Description: Centimetre-wide, weakly-zoned carbonate (inner) and quartz (outer) veins with clinozoisite selvage that replaced twinned centimetre-scale hornblende grains. Foliation in host-rock is defined by hornblende, and partially replaced by quartz and carbonate. Quartz and carbonate have lobate grain boundaries and are in part equigranular, but carbonate grains within veins are up to 100µm in diameter. Most intense chlorite alteration of hornblende is associated with fine-grained rutile. Small grains of minor Tn share lobate grain boundaries with quartz+carbonate and overprint small hornblende grains that have a common extinction angle. Po/Py is associated with quartz or K-feldspar (undulose extinction) and lesser chlorite. Paragenesis: Early hornblende defined a foliation; with unknown relationship between coarse and foliation-defining hornblende. Hb replaced by chlorite and overprinted by carbonate+Qtz+Tn+Po/Py in host and within veins. M400-023 Mineral abundance: talc – 35% hornblende – 24% carbonate – 20% chlorite – 20% rutile – 1% pyrrhotite – minor chalcopyrite – trace pyrite – trace
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Description: Talc arranged as blades within a sygmoidal habit within veins that have a Mg-chlorite selvage. Massive zones of talc+carbonate with local concentrations of carbonate. Rims of hornblende and where it is interstitial to large grains have been altered to chlorite. Rutile is concentrated within hornblende+chlorite zones. Bleached zones in non-polarized transmitted light represent carbonate+talc alteration of hornblende. Minor pyrrhotite and intergrown Cpy+Py are throughout carbonate+talc zones. Paragenesis: Early Hb altered to chlorite+rutile and carbonate+talc. M400-024 Mineral abundance: quartz – 60% plagioclase – 30% hornblende – 5% chlorite – 2% sericite – 2% biotite – 1% carbonate – minor titanite – minor ilmenite – minor Description: Within the felsic component, aligned hornblende defines a foliation that wraps around plagioclase phenocrysts. Plagioclase phenocrysts are recrystallised with subgrains of albite? and quartz. Rare aggregates of Hb up to 3mm long. groundmass is composed of predominantly quartz and lesser plagioclase. Titanite grains are associated with Hb and contain inclusions of ilmenite. Minor seritization of feldspar and cross-cutting carbonate veins/replacement of Hb. Large Hb grains up to 2mm in length are predominantly restricted to mafic contacts. Biotite defines a foliation within the mafic/ultramafic host that is partially to strongly converted to chlorite, and restricted to Hb rims and rare veins within the felsic host. Paragenesis: Plagioclase, K-feldspar and rare mafic phenocrysts were partially to completely recrystallised during alteration associated with the development of a Hb+Bt foliation. Titanite+ilmenite appear to be syn-post Hb. Carbonate veins, chlorite and sericite represent a later phase of ateration. M400-025 Mineral abundance: hornblende – 40% plagioclase – 30% chlorite – 15% quartz – 5% pyrrhotite – 5% ilmenite – minor Description: Hornblende, plagioclase and ilmenite are intergrown in an equigranular, massive texture. Hb is also within veins and a large plagioclase-bearing vein with needle-like Hb protrudes from vein walls. Anhedral titanite is restricted to rims of the plagioclase vein, and at the intersection of Hb-filled vein sets. In contrast to Hb that is distal to veins, vein-associated Hb is free of ilmenite inclusions. Late chlorite+quartz-filled fractures cross-cut Hb+plagioclase. Fractures/foliations also follow pre-existing Hb-filled veins. Po is spatially associated with Chl, quartz and minor carbonate. Paragenesis: Metamorphic Hb+plagioclase+Ilm was overprinted by plagioclase+Hb+Tn-filled veins. The veins were in turn overprinted by Chl+Qtz+Po±carbonate-filled fractures and veins
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M400-026 Mineral abundance: hornblende – 60% plagioclase – 25% quartz – 5% chlorite – 4% titanite – 5% pyrrhotite – 1% Description: Outlines of 1mm-sized Hb grains are preserved by aggregates of small Hb lathes. Part of the thin section contains aligned Hb and plagioclase/quartz that defines a foliation, and the other part contain relatively coarse, needle-like Hb and intergrown plagioclase and titanite arranged in an acicular texture. There is a corresponding decrease in the grainsize of Hb, plagioclase and Tn outside of the coarsest fraction, but an increase in abundance of Hb and Tn relative to plagioclase. Po is predominantly contained within relatively coarse units of plagioclase+Hb+Tn. Complete replacement of hornblende to chlorite is restricted to the margins of a few Po grains, with weak to no replacement surrounding Po being the general case. Quartz in coarser cross-cut plagioclase+Hb grain boundaries. Minor sericitization of plagioclase. Paragenesis: Metamorphic amphibole+plagioclase was replaced by hydrothermal hornblende+plagioclase+Tn, with the latter associated with foliation development and vein formation. Po is associated with minor retrogression of Hb to Chl, and is temporally related to Qtz. M400-027 Mineral abundance: chlorite – 30% carbonate – 25% hornblende – 20% plagioclase – 10% quartz – 8% pyrrhotite – 5% titanite – 1% rutile – 1% arsenopyrite – minor sericite - ? Description: Acicular Hb+Tn and plagioclase was weakly to completely replaced by Fe-Chl and carbonate, respectively. Pyrrhotite is in much greater abundance than in M400-026, and is predominantly spatially associated with the coarsest Hb fraction. Relict plagioclase is partially carbonatized and/or sericitized. Minor, coarse Tn is associated with Hb+carbonate+plagioclase within veins, and lesser, altered fine-grained Tn in the matrix is associated with Hb only. Hornblende is the most well-preserved within veins, where rims are weakly altered. Fine-grained carbonate within the core, and Chl at the rim of veins that cross-cut preserved Hb+plagioclase fabrics, also locally contain acicular prehnite. Fine-grained rutile is associated with areas of intensely chloritized Hb. Quartz is within the fine-grained groundmass and within veins. Paragenesis: Hb+plagioclase+Tn were replaced by chlorite and carbonate. Increasing Chl and carbonate alteration is associated with an increase in Po. Late carbonate+Chl+Trm veins cross-cut early Hb+plagioclase fabrics and possibly contain a different carbonate species. M400-028 Mineral abundance: actinolite – 60% carbonate – 19% plagioclase – 18% leucoxene – 2%
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sulphide – 1% K-feldspar – minor clinozoisite – minor Description: Fine-grained, acicular actinolite defines a foliation along with quartz. Zones of carbonate and minor K-feldspar replaced actinolite and quartz. Leucoxene and sulphide aligned parallel to foliation but overprint actinolite grain boundaries. Carbonate+K-feldspar-filled vein cross-cut the actinolite foliation. Czo rims altered actinolite within vein selvedge. Paragenesis: Actinolite+Ilm+plagioclase defined the early fabric that was replaced in part by carbonate+K-feldspar+sulphide, but ilmenite was completely replaced by leucoxene. M400-029 Mineral abundance: quartz – 40% hornblende – 27% carbonate – 20% biotite – 5% rutile – 2% chlorite – 5% pyrrhotite – 1% Description: Coarse hornblende or actinolite within layers are dispersed by overprinting carbonate and chlorite veins and a biotite-rich zone. Hornblende is partially to completely replaced by inclusions of quartz and carbonate. Biotite +chlorite+quartz-filled fractures cross-cut large hornblende grains. Within the biotite zone, biotite+rutile replaced the rims of hornblende and formed a foliation. Biotite rims were in turn replaced by chlorite. Relict, equant grains of ilmenite? were replaced by fine-grained rutile throughout the coarse hornblende zone. Biotite and chlorite are also intergrown with carbonate in veins. Direct replacement of hornblende by chlorite+rutile. Pyrrhotite is weakly associated with quartz+carbonate veins/replacement and the edges of altered zones. Paragenesis: Early metamorphic hornblende within granophyric dolerite was replaced by biotite+carbonate+quartz+chlorite+rutile+pyrrhotite. Quartz+carbonate that is interstitial to hornblende is possibly due to replacement of plagioclase. M400-030 Mineral abundance: carbonatized actinolite – 45% carbonate – 25% Mg-chlorite – 8% prehnite – 8% quartz – 5% rutile – 5% Fe-chlorite – 2% pyrite – 2% Description: Layers of coarse actinolite+Mg-chlorite+rutile+carbonate, carbonate+Mg-chlorite+rutile, partially-altered actinolite, and actinolite+quartz, were overprinted by multiple orientations of fine- to medium-grained carbonate+prehnite veins with Mg-chlorite rims. The perimeter of relict actinolite veins transgresses a weak layer-parallel foliation defined by actinolite. Discrete layer-parallel zones of Fe-chlorite+rutile after actinolite with some associated with a hybrid foliation/vein. Coarse, subhedral pyrite is associated with carbonate+prehnite veins. Paragenesis:
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Actinolite+quartz foliation was cross-cut/replaced by hornblende+plagioclase veins. The whole rock was then replaced by Mg-chlorite+rutile+carbonate. latest carbonate+prehnite+Mg-chlorite veins were associated with the alteration of actinolite to Fe-chlorite+rutile. M400-031 Mineral abundance: quartz – 30% carbonate – 20% hornblende – 20% biotite – 13% plagioclase – 7% pyrrhotite – 3% clinozoisite – 2% arsenopyrite – 2% rutile – 2% titanite – 1% pyrite/chalcopyrite – trace Description: Coarse hornblende+plagioclase up to 3mm in size was partially to completely replaced by small grains of quartz and carbonate. M400-032 Mineral abundance: amphibole – 60% tourmaline – 20% carbonate – 15% plagioclase – 2% leucoxene/rutile – 2% quartz – 1% ilmenite – trace M400-033 Mineral abundance: quartz – 30% carbonate – 20% clinozoisite – 18% hornblende – 17% prehnite – 10% chlorite – 2% pyrrhotite – 2% rutile – 1% arsenopyrite – minor chalcopyrite – trace M400-034 Mineral abundance: carbonate – 52% hornblende – 30% plagioclase – 10% chlorite – 5% tourmaline – 2% rutile/ilmenite – 1% opaques – minor quartz – minor titanite – trace M400-035 Mineral abundance:
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plagioclase – 35% hornblende – 25% biotite – 15% carbonate – 10% rutile – 5% quartz – 5% opaques – 3% titanite – 2% sericite? – mnr M400-036 Mineral abundance: quartz – 30% plagioclase – 21% white mica – 20% biotite – 10% opaques – 4% tourmaline – 3% amphibole – 3% titanite – 3% chlorite – 3% carbonate – 3% M400-037 Mineral abundance: amphibole – 75% clinozoisite – 15% quartz – 4% plagioclase – 3% opaques – 2% titanite – 1% carbonate – minor M400-038 Mineral abundance: amphibole – 75% carbonate – 7% clinozoisite – 5% chlorite – 5% plagioclase – 4% rutile – 3% opaques – 1% M400-039 Mineral abundance: amphibole – 54% tourmaline – 15% biotite – 15% chlorite – 10% clinozoisite – 5% opaques – 1% M400-040 Mineral abundance: amphibole – 50% plagioclase – 50% M400-041 Mineral abundance: amphibole – 40%
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carbonate – 40% chlorite – 20% M400-042 Mineral abundance: carbonate – 40% chlorite – 30% amphibole – 20% M400-043 Mineral abundance: chlorite – 45% carbonate – 45% carbonatized amphibole – 10% M400-044 Mineral abundance: amphibole – 50% plagioclase – 25% quartz – 25% M400-045 Mineral abundance: amphibole – 70% plagioclase – 8% biotite – 5% carbonate – 5% quartz – 5% clinozoisite – 5% opaques – 2% M400-046 Mineral abundance: biotite – 70% carbonate – 15% opaques – 8% carbonatized amphibole – 5% opaques – 2% M400-047 Mineral abundance: plagioclase – 50% quartz – 20% amphibole – 15% biotite – 5% garnet – 5% clinozoisite – 2% apatite – 2% opaques – 1%
Hannans North petrographic descriptions M400-001 Mineral abundance: chlorite – 40% quartz – 30 % epidote – 10% carbonate – 10% magnetite – 3% rutile/leucoxene – 6%
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pyrite – 1% Description: Matrix of fine-grained quartz±carbonate+epidote is intergrown with chlorite, and up to 500µm in diameter angular quartz grains, all of which (excluding quartz) are partially to strongly obscured by titanium staining (fine-grained rutile?). Evidence of relict magnetite euhedra replaced in part by leucoxene, and pyrite replaced by chlorite. Fractures that are associated with clear epidote+calcite-filled veins, cross-cut magnetite+pyrite. Paragenesis: Early magnetite+pyrite altered by late epidote+calcite+leucoxene in veins and groundmass. Unknown origin of angular quartz fragments except perhaps from original volcanic rock? Completely unaltered veins versus slightly strained matrix suggests ongoing late alteration with very late-stage veins. M400-002 Mineral abundance: carbonate – 60% chlorite – 12% magnetite – 10% actinolite – 5% quartz – 5% plagioclase – 5% pyrite – 3% epidote – trace Description: Magnetite inclusions within large elongate aggregates of pyrite grains aligned parallel to vein margins. Plagioclase lathes partially to strongly replaced by fine-grained carbonate and fine-grained to 500µm-long fibrous actinolite and chlorite. Carbonate is up 1mm in diameter within a cm-scale vein and foliated chlorite zone, and is associated with chlorite-replacement of magnetite and epidote in late chlorite-filled fractures. Paragenesis: Early magnetite+plagioclase+other precursor (hornblende?) was replaced by chlorite+actinolite+pyrite+carbonate±epidote. M400-003 Mineral abundance: epidote – 25% quartz – 25% chlorite – 20% carbonate – 20% magnetite – 10% chalcopyrite/pyrite – minor Description: Groundmass of fine-grained, needle-like chlorite+quartz, interleaved with sections of massive chlorite. Relict plagioclase lathes replaced by fine-grained carbonate. Coarse-grained carbonate+quartz+euhedral epidote in veins. Sections of complete replacement of host by epidote+quartz. Fine-grained to coarse euhedral magnetite along the perimeter of veins most closely associated with massive chlorite. Disseminated magnetite throughout the rest of the matrix. Monomineralic veins of chlorite and epidote mutually cross-cut. Chalcopyrite and pyrite are intergrown. Paragenesis: Primary plagioclase was replaced by carbonate and metamorphic? fine-grained actinolite was replaced by chlorite. Epidote+chlorite+quartz+magnetite+minor chalcopyrite/pyrite are within veins and also replaced all other wall-rock minerals. M400-004
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Mineral abundance: quartz – 30% carbonate – 30% white mica – 20% chlorite – 10% tourmaline – 4% leucoxene – 3% pyrite – 3% ilmenite/magnetite – minor Description: Fine-grained sericite+carbonate+quartz groundmass, with partial replacement of plagioclase lathes. Carbonate+quartz intergrown with chlorite in groundmass, and former also coarse within veins. Fine-grained muscovite also within narrow veins?/layering? Tourmaline is perpendicular to long axis – with partially carbonate-replaced rims – are dispersed throughout the rock. Leucoxene with partial preservation of ilmenite or latter magnetite replacement along crystallographic orientations. Coarse, euhedral pyrite. Paragenesis: Plagioclase+ilmenite are early grains that were replaced by carbonate+quartz+sericite+tourmaline+pyrite+leucoxene assemblage.
Bullant petrographic descriptions M400-005 Mineral Abundance: amphibole – 50% quartz – 20% epidote – 10% chlorite – 10% carbonate – 5% rutile – 5% pyrrhotite – minor chalcopyrite – trace Description: Dominantly fine-grained equigranular amphibole and relict disseminated ilmenite? with rims replaced by interstitial rutile+chlorite. Matrix also contains quartz. Quartz+epidote+lesser carbonate in veins that also contain intergrown pyrrhotite+chalcopyrite. Inconsequential sulphide outside of veins. Paragenesis: Metamorphic actinolite?+ilmenite replaced/cross-cut by chlorite + rutile and epidote, quartz, pyrrhotite, chalcopyrite, carbonate-filled veins. M400-006 Mineral abundance: carbonate – 35% chlorite – 35% quartz – 30% pyrrhotite/chalcopyrite – minor tremolite – minor Description: Asymmetric/sigmoidal lithons of quartz+chlorite, enveloped by foliations defined by very fine-grained rutile? after biotite? Fine-grained chlorite after tremolite: the latter is completely replaced but there is rare evidence of characteristic birefringence. Cross-cutting medium-grained, equigranular carbonate+quartz veins. Minor intergrown pyrrhotite+chalcopyrite. Paragenesis:
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Early tremolite widespread through matrix, with a biotite foliation of unknown (early) timing. Chlorite+rutile+carbonate+quartz+pyrrhotite+chalcopyrite is a late-stage replacement/vein assemblage. M400-007 Mineral abundance: carbonate – 40% chlorite – 40% quartz – 18% tourmaline – 2% pyrrhotite – minor chalcopyrite – trace Description: Very fine-grained to 100µm-sized chlorite after tremolite. Weakly-developed differentiated layering of very fine-grained to coarse-grained relict tremolite, and also quartz. Carbonate grains as static overgrowths of matrix, but also within small (µm-scale) and large (cm-scale) veins. Tourmaline grains are static overgrowths of tremolite matrix, and partially replaced by carbonate. Minor pyrrhotite+chalcopyrite is associated with matrix carbonate. Paragenesis: Earliest tremolite+quartz layering was replaced by chlorite+carbonate+tourmaline+pyrrhotite+chalcopyrite and cross-cut by carbonate veins. M400-008 Mineral abundance: quartz – 30% carbonate – 20% biotite – 20% hornblende – 12% chlorite – 10% plagioclase – 5% pyrrhotite – 3% chalcopyrite – trace Description: Equigranular biotite defines a weak to moderately strong foliation and is spatially associated with plagioclase and carbonate within a very fine-grained quartz+chlorite groundmass. Chlorite partially replaced biotite rims and completely replaced selected hornblende grains. Pyrrhotite ± chalcopyrite occurs with carbonate and overprints hornblende grains. Paragenesis: Biotite+plagioclase foliation and quartz was pre-syn static hornblende grains. Carbonate was syn-post biotite, and chlorite replaced biotite+hornblende. Pyrrhotite+chalcopyrite+carbonate was the latest alteration phase. M400-009 Mineral abundance: carbonate – 45% quartz – 35% hornblende – 7% chlorite – 5% plagioclase – 5% pyrrhotite – 3% muscovite – minor chalcopyrite – trace Description: Alternate carbonate-rich and quartz+plagioclase+hornblende-rich zones. Carbonate is medium-grained, equigranular and xenomorphic. Quartz as fine-grained groundmass and to a lesser extent in
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veins with minor muscovite. Radial aggregates of neddle-like hornblende is stable in groundmass of quartz+plagioclase, but unstable within carbonate where it converts to chlorite+carbonate. A chlorite foliation is parallel to carbonate and quartz+plagioclase+hornblende contacts, and is in equilibrium with carbonate. Localized quartz re-crystalization surrounding pyrrhotite grains that overprint all except carbonate+chlorite, but generally absent from carbonate zones. Paragenesis: Hornblende+plagioclase+quartz was overprinted by carbonate+chlorite+pyrrhotite+chalcopyrite, with late quartz+muscovite veins synchronous with the latter.
Bullant petrographic descriptions M400-127 Mineral abundance: plagioclase – 25% chlorite – 25% carbonate – 20% biotite – 15% quartz – 5% rutile – 5% pyrrhotite/pyrite – 5% Description: Strongly-foliated chlorite+rutile and localised concentrations of foliated biotite particularly at vein margins. Veins contain plagioclase, quartz, carbonate, pyrrhotite/pyrite and chlorite, with biotite intergrown with the latter at foliated vein margins (selvage). Stubby plagioclase within veins is distinct from elongate, acicular (at times aligned parallel to the dominant foliation) plagioclase within the matrix. Both plagioclase phases were replaced by carbonate. Paragenesis: Early actinolite+plagioclase matrix was deformed and altered by chlorite+biotite+rutile and intruded by chlorite+plagioclase+quartz+carbonate +pyrrhotite veins. Carbonate+pyrrhotite was syn-post vein-hosted plagioclase. M400-128 Mineral abundance: plagioclase – 27% carbonate – 23% quartz – 12% biotite – 10% amphibole – 10% chlorite – 8% pyrrhotite – 8% rutile – 2% Description: Radial aggregates of amphibole co-exist with coarse plagioclase and quartz that are overprinted by narrow, fingering veins comprised of fine-grained quartz, feldspar and carbonate. There is also static overgrowth of coarse plagioclase and quartz by carbonate and pyrrhotite. Biotite selvage to the vein is intergrown with amphibole and is partially replaced by chlorite. Foliated plagioclase with lesser chlorite+rutile matrix/wall-rock was statically overgrown by coarse, prismatic amphibole, but amphibole cores were replaced by chlorite+rutile. Paragenesis: Amphibole+plagioclase+quartz vein intruded the foliated plagioclase+biotite?/ actinolite? rock, which was then altered by a further vein set of carbonate+quartz+feldspar+pyrrhotite that selectively chloritized the biotite and amphibole cores.
Wallaby petrographic descriptions
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WB0801CD 116.0 m Mineral abundance: plagioclase – 30% carbonate – 30% amphibole – 20% rutile – 10% epidote – 5% magnetite – 4% pyrite – 1% chalcopyrite – trace Description: Carbonate selectively/partially replaced amphibole+plagioclase. Epidote within confined accumulations within clasts of intergrown acicular amphibole+plagioclase, intergrown with plagioclase+carbonate+quartz within small circular infill, and within minor, interclast foliations containing amphibole? of blue colour/birefringence. Epidote overgrew large, untwinned plagioclase along with quartz+carbonate along relict cleavage planes, but is intergrown with stubby, albite-twinned plagioclase. Epidote in places has the same habit as relict amphibole (photomicrographs; WB0801CD_116m_1Trans&XPol and WB0801CD_116m_2Trans&XPol), and is intergrown with subrounded rutile? grains. Relict amphibole cleavage and grain shape are preserved within epidote, and relatively light patches compared to the diagnostic apple-green epidote colour in transmitted light represents partially-altered amphibole that is also indicated by relatively lower birefringence colours compared to epidote. Amphibole was replaced by predominantly carbonate or rutile, and alteration domains were broadly defined by clast type. Carbonate partially to completely replaced amphibole, and very fine-grained rutile replaced amphibole cores. A very narrow rim of epidote accompanied the rutile alteration. Magnetite and pyrite are fine-grained and disseminated with irregular grain edges, and show examples of mutual overprinting. Paragenesis: Early amphibole+plagioclase were replaced by epidote+quartz+rutile+carbonate plus a secondary phase of plagioclase. Opaques do not have a clear relationship, but appear late. WB0801CD 128.5 m Mineral abundance: carbonate – 30% actinolite/tremolite – 30% quartz – 20% plagioclase – 15% magnetite – 4% pyrite – 1% Description: Layers of fibrous actinolite/tremolite with grains aligned perpendicular to vein walls. Elongate, but comparatively stubby amphibole grains within fine-grained acicular matrix, and coarser amphibole associated with carbonate especially where the latter was plucked out during thin section prep (unpolished zones with cleavage intersection). Carbonate overgrew amphibole within the matrix, but predominantly at the interface of quartz and actinolite layers. Quartz is confined to layers within the vein and is equigranular and has irregular but mainly triple-point grain boundaries. Some clasts in host rock have acicular plagioclase and others massive growth of stubby grains within aggregates. Disseminated magnetite and pyrite throughout, but predominantly associate with carbonate alteration within actinolite zones. Paragenesis: Amphibole+plagioclase within clasts/host rock was coeval with development of vein associated actinolite. Actinolite was replaced by carbonate in association with quartz+magnetite+pyrite. WB0801CD 790.1 m Mineral abundance: amphibole – 42% carbonate – 25%
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plagioclase – 15% quartz – 5% epidote – 5% ilmenite/rutile – 5% pyrite – 2% magnetite – 1% Description: Relict acicular plagioclase in some clasts. Magnetite and tarnished pyrite grains are rimmed by ilmenite/rutile. Elongate ilmenite is also widespread throughout the matrix. Epidote is associated with magnetite and pyrite and overprinted amphibole. Epidote predominantly occurs intergrown with quartz and carbonate and is in highest abundance adjacent to amphibole zones. Titanite (partially altered?) is intergrown with amphibole in matrix. Carbonate partially to completely replaced amphibole. Where amphibole is partially replaced, the birefringence verges toward higher order colours. Paragenesis: Early amphibole+titanite±plagioclase was replaced by epidote. Carbonate+quartz is intergrown with epidote but the association of pyrite and magnetite with epidote and carbonate+quartz with ilmenite suggest that carbonate and quartz is syn-post epidote. WB0801CD 233.0 m Mineral abundance: plagioclase – 30% carbonate – 20% chlorite – 20% biotite – 10% pyrite – 15% magnetite – 3% rutile – 2% tourmaline – minor Description: Fine- to medium-grained plagioclase+chlorite matrix was cross-cut by veins that have localised concentrations of biotite and lesser tourmaline as selvage and within foliations. Acicular plagioclase in matrix was x-cut by vein-hosted plagioclase+biotite that in turn was partially altered by carbonate+chlorite. Intergrown plagioclase (albite), carbonate and chlorite (primary) within veins cross cut pre-existing plagioclase+biotite, but occupied the same large vein, which is contained between bordering biotite+tourmaline foliations. Pyrite and magnetite grains are disseminated throughout the matrix, with some pyrite containing magnetite inclusions. Pyrite is the sole opaque associated with the biotite-tourmaline foliation, and is coarsest in association with carbonate+plagioclase veins. Paragenesis: Early acicular plagioclase+actinolite? was replaced and overprinted by plagioclase+biotite+tourmaline+magnetite, which was overprinted/replaced by albite+carbonate+chlorite+pyrite. WB0801CD 236.9 m Mineral abundance: carbonate – 35% biotite – 13% amphibole – 12% quartz – 10% plagioclase – 9% chlorite – 8% rutile – 7% magnetite – 3% pyrite – 3% chalcopyrite – minor Description:
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Biotite as selvage or a weak foliation at perimeter of carbonate+quartz+amphibole+plagioclase±titanite-filled vein that cross-cuts fine-grained acicular relict actinolite(now chlorite)+plagioclase within primary clasts. Magnetite as selvage to veins including intergrown with amphibole and carbonate that border a network of angular, equigranular aggregates of quartz within the central part of the vein. Rutile is confined to the actinolite+plagioclase within clasts. Pyrite predominantly restricted to the vein and most grains contain magnetite inclusions. Paragenesis: Early plagioclase+actinolite in clasts that were cross-cut by amphibole+plagioclase±titanite-filled veins with syn-biotite/magnetite foliation/selvage. Pyrite and rutile are associated with the replacement of plagioclase and amphibole by carbonate+quartz in veins and carbonate+chlorite within the matrix. WB0801CD 377.5 m Mineral abundance: carbonate – 30% biotite – 15% plagioclase – 14% chlorite – 12% quartz – 10% amphibole – 5% clinozoisite – 4% pyrite – 5% rutile – 3% tremolite/prehnite – 2% Description: Biotite+chlorite+plagioclase+carbonate+rutile/ilmenite dominate the matrix. Biotite is intergrown with a colourless mineral within veins (high relief, 2nd order interference colours, twinned, bladed) that could be tremolite/prehnite/pumpellyite. Much of the original acicular plagioclase matrix (within clasts) has been altered to prehnite? and clinozoisite. The latter could also be amphibole altered to clinozoisite. Biotite is mainly in veins, within an increasing ratio of chlorite:biotite away from former. Chlorite replaced biotite in the vicinity of carbonate+quartz. The single 0.5 cm-wide vein is filled with coarse-grained quartz+albite with relatively fine-grained carbonate+quartz+albite rims, including partially chlorite-altered amphibole. Coarsest pyrite is associated with carbonate+quartz+albite in veins. Rutile and rare magnetite is disseminated throughout the matrix. Paragenesis: Biotite and amphibole were replaced by chlorite and clinozoisite within the matrix, respectively. Amphibole and biotite were replaced by chlorite within veins. Carbonate+quartz replaced plagioclase. Rutile and pyrite are related to latest carbonate alteration. WB0801CD 378.6 m Mineral abundance: biotite – 35% plagioclase – 15% rutile – 13% chlorite – 12% carbonate – 10% pyrite – 8% amphibole – 4% quartz – 3% Description: All of the thin section matrix (within large mafic clast) is comprised of acicular plagioclase variably altered to rutile, carbonate and prehnite. The dominant mafic mineral within the groundmass is biotite that forms a selvage to veins. Chlorite is a replacement product of biotite especially adjacent to prehnite+rutile+pyrite. Very fine-grained biotite and amphibole along with carbonate is within most veins. Prehnite within matrix is associated with pyrite. The widest vein is comprised of quartz+plagioclase. Rutile is concentrated within relatively-unaltered matrix. Pyrite is homogeneously distributed throughout the thin section.
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Paragenesis: Actinolite within (none left) matrix was completely altered to biotite during introduction of amphibole+biotite+plagioclase±quartz-filled veins. Carbonate+chlorite+prehnite+pyrite+rutile replaced former alteration associated with veining including partially replacing plagioclase in matrix. WB0801CD 403.8m Mineral abundance: plagioclase – 60% biotite – 15% white mica – 10% carbonate – 8% pyrite – 4% quartz - magnetite – 2% rutile – 1% Description: Most of the matrix is comprised of acicular plagioclase that is partially altered to fine-grained white mica or carbonate. Quartz grains throughout the thin section are subangular/subhedral and 250-500 µm in diameter. Clasts with relict pyroxene grain shapes are predominantly comprised of very fine-grained carbonate+biotite+rutile, but in approximately 50% of cases, medium-grained (100µm) intergrown biotite+muscovite overgrew the former. Coarsest carbonate+pyrite as well as muscovite+quartz (with magnetite and chalcopyrite inclusions) are hosted within veins. Pyrite and magnetite grains are disseminated throughout the matrix. Paragenesis: Pyroxene phenocrysts within plagioclase matrix were replaced by biotite+muscovite and carbonate+muscovite, respectively. Magnetite was coeval with biotite and pyrite/chalcopyrite was synchronous with latest carbonate+quartz+muscovite veins. WB0801CD 426.1 m Mineral abundance: plagioclase - 30% chlorite – 28% carbonate – 17% pyrite – 8% quartz – 5% amphibole – 5% biotite – 3% rutile – 2% clinozoisite – 1% tourmaline – 1% Description: Relict hornblende within veins is almost completely altered to chlorite. Quartz within veins is in equilibrium with carbonate and pyrite. Coarse albite within veins is partially altered to carbonate where minor veins cross-cut and at grain margins. Amphibole is either partially-altered actinolite or tremolite, and is altered to clinozoisite at one end of the thin section. Elongate tremolite? and tourmaline grains are intergrown with chlorite and lesser biotite within an intense foliation. Carbonate is predominantly within veins with pyrite, but also partially altered acicular plagioclase within the matrix. Paragenesis: Plagioclase+actinolite(mafic mineral?) matrix altered by hornblende including hornblende+plagioclase veins. Hornblende+plagioclase was then statically-altered to clinozoisite+carbonate, and cross-cut by chlorite+biotite+tremolite?+tourmaline +pyrite within foliations. A second phase of plagioclase (albite) and syn-post carbonate+pyrite within veins altered/cross-cut earlier hornblende+plagioclase. WB0801CD 470.8 m Mineral abundance:
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amphibole – 30% rutile – 20% anhydrite – 15% plagioclase – 10% epidote – 10% quartz – 10% garnet – 2% sulphide – 2% magnetite? Description: Acicular actinolite+plagioclase matrix was directly overprinted by vein-hosted amphibole+quartz+plagioclase?, and also by rutile, carbonate and lesser epidote. Ovoid-shaped garnet aggregates are strongly altered by epidote, particularly at their margins, which is associated with anhydrite+quartz veins that cross-cut the former and the vein-hosted amphibole. Quartz, carbonate, rutile, anhydrite and epidote form a 2-3 cm-wide selvage to the vein array that contain the same minerals. Epidote, carbonate and quartz are directly associated with sulphide. To determine opaque phases. Paragenesis: Acicular plagioclase+actinolite matrix overprinted by initial hornblende+quartz veins and vein-hosted? garnet. Quartz, carbonate, rutile, anhydrite, epidote and pyrite overprinted early alteration and replaced veins that hosted garnet/hornblende. WB0801CD 610.65 m Mineral abundance: quartz – 60% carbonate – 25% amphibole – 8% magnetite – 3% pyrite – 2% biotite – 1% plagioclase – 1% chlorite – minor Description: Nodules contain relict plagioclase, carbonate as a partial replacement of the former, concentric rings of magnetite+pyrite (to describe fully later), bladed and randomly-oriented hornblende, and a concentration of carbonate and biotite at the perimeters. Equigranular, recrystallized quartz dominates the space between nodules. One chlorite- (after hornblende), quartz- and carbonate-filled vein fills one corner of the thin section and is in equilibrium with the quartz matrix. Paragenesis: Plagioclase plus an unknown mafic mineral was replaced by hornblende+biotite. Carbonate altered nodule rims during later mineral replacement that coincided with quartz, chlorite, magnetite and pyrite introduction. WB0801CD 790.1 m Mineral abundance: carbonate – 25% white mica – 25% chlorite – 20% quartz – 10% leucoxene – 10% magnetite – 5% pyrite – 3% plagioclase – 2% Description:
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Sygmoidal clasts of carbonate and lesser plagioclase are enveloped by a matrix of foliated white mica and chlorite. Fine-grained quartz is concentrated within tails of clasts, and as a recrystallization product of the same clasts, plus dominates part of the thin section matrix where it surrounds white mica (no chlorite) dominated oval-shaped aggregates. Subhedral pyrite contain chlorite+quartz-filled tails similarly to carbonate clasts. Carbonate-filled veins transgresses most of the penetrative fabric, but is cross-cut by quartz+carbonate+chlorite+white mica+pyrite+magnetite-filled foliations and veins. Leucoxene are contained within and aligned parallel to the dominant white mica+chlorite foliation. Fine-grained magnetite overprints the clasts and matrix, are parallel to the dominant foliation, but is also aligned in trains that are discordant to the former. Magnetite rims subhedral pyrite in veins and matrix. Paragenesis: Plagioclase phenocrysts within ilmenite-rich dolerite was overprinted by carbonate and leucoxene, respectively. A chlorite+white mica+quartz foliation deformed the dolerite, which was coeval with the development of carbonate+quartz+chlorite+pyrite +magnetite-filled veins. WB0801CD 847.8 m Mineral abundance: white mica – 25% carbonate – 25% quartz – 20% plagioclase – 10% chlorite – 10% magnetite/ilmenite – 7% pyrite (tarnished) – 3% Description: Mainly defined by a fine-grained white-mica+carbonate+quartz foliation with rare quartz and plagioclase clasts. Chlorite is concentrated as a foliation within a few horizons, and within aligned aggregates that are indicative of replaced amphibole/biotite porphyroblasts. Carbonate is in the form of needle-like grains that are preserved as acicular plagioclase within spherical aggregates at one end of thin section. Quartz+carbonate+pyrite+magnetite+white mica (relatively coarse-grained) ± chlorite is contained within veins and lesser foliations. Pyrite and magnetite are predominantly spatially separated, and occupy the ends and middle of the thin section, respectively. Paragenesis: Acicular plagioclase replaced by carbonate and deformed by white mica+chlorite foliations and quartz+pyrite+magnetite veins. WB0801CD 864.4 m Mineral abundance: carbonate – 35% quartz – 35% white mica – 11% chlorite – 10% plagioclase – 5% tourmaline – 2% magnetite/ilmenite – 1% pyrite – 1% Description: Plentiful, closely spaced clasts after plagioclase – partially sericitized in grain cores and almost completely converted to carbonate – that are aligned parallel to a dominantly quartz and lesser white mica and chlorite foliation, although locally high concentrations of latter minerals. Partially- to strongly-altered tourmaline is concentrated along a few discrete layers, including the periphery of a cm-wide carbonate+quartz vein. Possible plagioclase within vein. Tourmaline was replaced by (Fe?) chlorite. Pyrite is concentrated around carbonate (veins). Magnetite or fine-grained elongate ilmenite? is mainly confined to chlorite/tourmaline zones. Paragenesis:
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Early plagioclase-rich rock was cross-cut by plagioclase+quartz veins that have tourmaline selvage. Carbonate+white+quartz mica altered both generations of plagioclase and chlorite associated with former replaced tourmaline. WB0801CD 1141.1 m Mineral abundance: carbonate – 25% white mica – 25% quartz – 20% chloritoid – 15% chlorite – 5% pyrrhotite – 7% magnetite – 2% chalcopyrite – 1% Description: Rosettes of stubby, twinned chloritoid are concentrated along white mica foliation planes and at the margins of coarse to fine-grained quartz and carbonate aggregates and veins. The spheroidal, cm-scale aggregates consist of very fine-grained white mica+carbonate+chlorite+euhedral disseminated magnetite, or very fine-grained quartz and lesser carbonate+pyrrhotite+chalcopyrite. Coarse-grained quartz+carbonate veins contain most of the pyrrhotite, but a significant proportion is associated the replacement of chloritoid. Chlorite also partially replaced chloritoid. White mica foliation partly cross-cuts chloritoid. Magnetite is restricted only one of the spheroidal aggregates, whereas pyrrhotite is widespread but did not develop in the former. Paragenesis: Pebble conglomerate was replaced by a combination of chloritoid, quartz, carbonate and white mica, but chlorite is more co-stable with the latter three minerals. Chloritoid may have been initially stable with the white mica assemblage, but progressive development of the foliation and associated alteration saw the development of chlorite as the stable ferromagnesian mineral. Quartz+carbonate veins may have contained plagioclase initially, but since converted to carbonate+quartz. WB0801CD 1145.5 m Mineral abundance: carbonate – 60% quartz – 20% white mica – 7% magnetite – 7% pyrrhotite – 5% chloritoid/amphibole? – 1% chalcopyrite – minor ilmenite – minor Description: One end of thin section is comprised of massive carbonate with disseminated grains of quartz and skeletal magnetite. Pyrrhotite+chalcopyrite overgrow the skeletal magnetite. The other end of the thin section is comprised of a >3 cm-diameter clast that has three distinct layers. The first layer consists of very fine-grained quartz+carbonate and interstitial pyrrhotite+chalcopyrite. The second layer has the same quartz+carbonate texture as the first, albeit a greater relative amount of carbonate to quartz, but contains a much higher percentage of opaques comprising equal amounts of intergrown magnetite+pyrrhotite±chalcopyrite. The third layer comprises predominantly carbonate and lesser quartz, and contains the coarsest magnetite in the thin section as the main opaque. Minor pyrrhotite is mainly included within the subhedral magnetite grains. White mica foliations and spatially associated chloritoid/amphibole? (in rosettes) anstomose between the two main domains described above. Minor zones of carbonate+quartz lie between the foliations. small grains of elongate ilmenite? are associated with the chloritoid+white mica foliations and perhaps retrogression of chloritoid to chlorite. Zoned quartz+carbonate+pyrrhotite veins cross-cut the cm-scale clasts. Paragenesis:
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Pebble conglomerate replaced by predominantly carbonate+quartz, with interstitial foliations associated with same alteration. Chloritoid is pre-syn the current alteration assemblage, which is similar to most amphibole. The different opaque components and timing relationships are due to the variable composition of the pebble clasts. WB0801CD 1175.1 m Mineral abundance: quartz – 68% carbonate – 15% magnetite – 8% chloritoid/amphibole? – 4% chlorite – 3% pyrrhotite – 2% arsenopyrite – 1% chalcopyrite – minor rutile – minor Description: Chloritoid/amphibole?+quartz foliation is altered to chlorite+quartz+rutile+pyrrhotite at margins adjacent to quartz+carbonate+magnetite+sulphide zones that consititute most of the thin section. Skeletal magnetite within foliated zone is overgrown by pyrrhotite+chalcopyrite, with the latter preserving the euhedral magnetite grain shapes. Coarse quartz grains with irregular grain boundaries lie inside of the foliated zone. Most of the thin section is composed of fine-grained quartz and lesser carbonate, with concentrated zones of magnetite and magnetite+carbonate that are aligned discordant to the foliation orientation. Outside of the foliated zone the dominant opaque is magnetite, with pyrrhotite+chalcopyrite as inclusions within the former. Most and especially the coarsest arsenopyrite grains are associated with the magnetite bands within the magnetite-hosted layering. Minor cases of magnetite as inclusions within arsenopyrite. Paragenesis: Still a question as to whether the equant, elongate dark green mineral is chloritoid or amphibole where it is partially/strongly altered to chlorite (to probe). Distinctive twinning gives it away as chloritoid where present, and also within chloritoid zone as defined by infrared spectra. Early amphibole/chloritoid foliation altered to chlorite; with static (no white mica) replacement of the former. The relative amount of and timing between sulphides and magnetite is controlled by the composition of the host rock, and also the overprinting, pyrrhotite-stable foliation. WB0801CD 1183.3 m Mineral abundance: quartz – 55% carbonate – 30% chloritoid – 5% chlorite – 3% pyrite – 3% magnetite – 2% pyrrhotite – 2% ilmenite – minor Description: Layers of variably-sized quartz+carbonate – each with different mineral ratios, are cross cut by discordant chlorite (after chloritoid; twinning) foliation zone containing coarse quartz clasts. Intergrown magnetite, pyrite and pyrrhotite are parallel to and within selected layers, but within the crosscutting foliation pyrite overgrew skeletal magnetite and pyrrhotite rims pyrite. Fine-grained, elongate ilmenite is restricted to chlorite zones. Carbonate selectively replaced chloritoid/chlorite. Paragenesis: Chloritoid zone cross-cut original layering. Carbonate+quartz+chlorite+opaques post-date chloritoid. Magnetite was replaced by pyrite and latest pyrrhotite. WB0801CD 1193.9 m
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Mineral abundance: carbonate – 50% chlorite (after chloritoid) – 30% white mica – 10% plagioclase – 7% quartz – 2% ilmenite/magnetite – 1% biotite? - minor pyrrhotite – minor pyrite/chalcopyrite – trace Description: Chloritoid grains are evenly distributed throughout the matrix and have a weak preferred alignment parallel to the dominant foliation defined by white mica; albeit the latter cross-cuts and deforms chloritoid. Chloritoid has been ubiquitously altered to chlorite – but the partial replacement has preserved strong twinning. Chloritoid is rimmed with ilmenite/rutile? where in contact with carbonate, and the latter sporadically replaced chloritoid. Carbonate and white mica within slightly discordant foliations/veins are iron-stained, but there is also potential biotite associated with these. Elongate ilmenite/magnetite? grains are evenly distributed throughout the matrix and are aligned approximately parallel to the dominant foliation. Sulphides are distributed randomly throughout the thin section. Paragenesis: White mica deformed chloritoid during progressive development of the dominant foliation within the rock, and also developed late foliations/veins at a discordant angle to the main fabric. Chlorite+ilmenite+carbonate replaced chloritoid during late foliation development. WB0801CD 1201.9 m Mineral abundance: white mica – 50% carbonate – 25% quartz – 20% ilmenite – 3% pyrrhotite – 1% amphibole (altered) – 1% arsenopyrite – minor Description: Strong foliation defined by white mica, quartz and elongate ilmenite (magnetite?), and static growth of carbonate that potentially replaced feldspar. Coarse-grained quartz+carbonate veins cross-cut the foliation. Fine-grained, radial aggregates of relict amphibole (actinolite?) are within the quartz+carbonate veins, but are predominantly at vein margins. Pyrrhotite grains overgrew the foliation and have a preferred orientation parallel to the foliation. Paragenesis: White mica+carbonate replaced a plagioclase-rich rock. Veins were originally quartz+plagioclase+amphibole but the latter two were replaced during latest alteration. Amphibole is partially replaced, not completely going to chlorite/carbonate.
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Appendix 4: SWIR & TIR Spectra of apatite (Mitchell collection)
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APPENDIX 4
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Appendix 5: Sample Catalogue
A-58
APPENDIX 5
Thin section Drill hole Depth (m) Sample ID Prospect microprobed ASD microFTIRM400-001 HND002 67.200 - Hannans NorthM400-002 HND002 93.200 - Hannans NorthM400-003 HND002 100.500 - Hannans NorthM400-004 HND002 126.500 - Hannans NorthM400-005 BUGD049 33.500 - BullantM400-006 BUGD049 91.200 - BullantM400-007 BUGD049 116.100 - BullantM400-008 BUGD049 181.000 - BullantM400-009 BUGD049 197.100 - BullantM400-010 UDD1420 83.973 J58798 BalticM400-011 UDD1420 242.302 J58803 BalticM400-012 UDD1420 254.902 J58806 BalticM400-013 UDD1420 266.946 J58808 BalticM400-014 UDD1420 267.049 J58809 BalticM400-015 UDD1420 268.002 J58810 BalticM400-016 UDD1420 313.893 J58811 BalticM400-017 UDD1420 314.132 J58812 BalticM400-018 UDD1420 324.819 J58813 BalticM400-019 UDD1420 346.176 J58814 BalticM400-020 UDD1420 440.714 J58817 BalticM400-021 UDD1420 459.766 J58820 BalticM400-022 UDD1420 475.549 J58821 BalticM400-023 UDD1420 484.906 J58822 BalticM400-024 UDD1420 497.600 J58823 BalticM400-025 UDD1510 59.154 J58824 TimorM400-026 UDD1510 143.287 J58825 TimorM400-027 UDD1510 144.035 J58826 TimorM400-028 UDD1510 158.067 J58828 TimorM400-029 UDD1510 170.006 J58830 TimorM400-030 UDD1510 195.829 J58832 TimorM400-031 UDD1510 217.798 J58833 TimorM400-032 UDD1510 235.978 J58834 TimorM400-033 UDD1510 239.578 J58835 TimorM400-034 UDD1510 249.184 J58836 TimorM400-035 UDD1508 159.888 J58839 TimorM400-036 UDD1508 163.090 J58840 TimorM400-037 UDD1508 166.298 J58841 TimorM400-038 UDD1508 210.370 J58843 TimorM400-039 UDD1508 250.093 J58845 TimorM400-040 UDD1508 253.117 J58847 TimorM400-041 PERCD8151A 387.969 J58848 Zone 114 (Pacific)M400-042 PERCD8151A 391.759 J58849 Zone 114 (Pacific)M400-043 PERCD8151A 410.076 J58850 Zone 114 (Pacific)M400-044 PERCD8151A 422.669 J58851 Zone 114 (Pacific)M400-045 PERCD8151A 423.494 J58852 Zone 114 (Pacific)M400-046 PERCD8151A 426.499 J58853 Zone 114 (Pacific)M400-047 PERCD8151A 428.911 J58854 Zone 114 (Pacific)M400-048 LARCD1027 307.400 M400-KR01 KrakenM400-049 LARCD1028 342.700 M400-KR03 Kraken
LARCD1029 81-82 M400-KR04 KrakenLARCD1029 90-91 M400-KR05 KrakenLARCD1029 91-92 M400-KR06 Kraken
M400-050
A-59
LARCD1029 99-100 M400-KR07 KrakenLARCD1029 102-103 M400-KR08 KrakenLARCD1029 115-116 M400-KR09 KrakenLARCD1029 125-126 M400-KR10 KrakenLARCD1029 228-229 M400-KR11 KrakenLARCD1029 243-244 M400-KR12 KrakenLARCD1029 282-283 M400-KR13 KrakenLARCD1027 254-255 M400-KR14 KrakenLARCD1027 263-264 M400-KR15 KrakenLARCD1027 266-267 M400-KR16 KrakenLARCD1027 278-279 M400-KR17 KrakenLARCD1027 280-281 M400-KR18 KrakenLARCD1027 295-296 M400-KR19 Kraken
M400-055 LARCD1007 176.100 M400-SY01 SylvesterM400-056 LARCD1007 194.700 M400-SY02 SylvesterM400-057 LARCD1005 112.400 M400-SY03 SylvesterM400-058 LARCD0921 222.000 M400-SY04 SylvesterM400-059 LARCD1004 194.450 M400-SY05 Sylvester
LARC1011 80-81 M400-SY06 SylvesterLARC1011 82-83 M400-SY07 SylvesterLARC1011 83-84 M400-SY08 SylvesterLARC1011 95-96 M400-SY09 SylvesterLARC1011 96-97 M400-SY10 SylvesterLARC1011 99-100 M400-SY11 SylvesterLARC1011 100-101 M400-SY12 SylvesterLARC1011 101-102 M400-SY13 SylvesterLARC1011 106-107 M400-SY14 SylvesterLARC1011 123-124 M400-SY15 SylvesterLARC1011 130-131 M400-SY16 SylvesterLARC1011 137-138 M400-SY17 SylvesterLARC0919 81-82 M400-SY18 SylvesterLARC0919 88-89 M400-SY19 SylvesterLARC0919 96-97 M400-SY20 SylvesterLARC0919 100-101 M400-SY21 SylvesterLARC0919 108-109 M400-SY22 SylvesterLARC0919 110-111 M400-SY23 SylvesterLARC0919 113-114 M400-SY24 SylvesterLARC0919 115-116 M400-SY25 SylvesterLARC0919 122-123 M400-SY26 SylvesterLARC0919 138-139 M400-SY27 SylvesterLARC0920 96-97 M400-SY28 SylvesterLARC0920 102-103 M400-SY29 SylvesterLARC0920 107-108 M400-SY30 SylvesterLARC0920 112-113 M400-SY31 SylvesterLARC0920 114-115 M400-SY32 SylvesterLARC0920 119-120 M400-SY33 SylvesterLARC0920 122-123 M400-SY34 SylvesterLARC0920 131-132 M400-SY35 SylvesterLARC0920 140-141 M400-SY36 SylvesterLARC0920 149-150 M400-SY37 SylvesterLARC0921 115-116 M400-SY39 SylvesterLARC0921 117-118 M400-SY40 SylvesterLARC0921 118-119 M400-SY41 SylvesterLARC0921 121-122 M400-SY42 SylvesterLARC0921 124-125 M400-SY43 SylvesterLARC0921 125-126 M400-SY44 Sylvester
M400-067
M400-068
M400-063
M400-064
M400-065
M400-066
M400-054
M400-060
M400-061
M400-062
M400-051
M400-052
M400-053
A-60
LARC0921 128-129 M400-SY45 SylvesterLARCD1007 108-109 M400-SY46 SylvesterLARCD1007 113-114 M400-SY47 SylvesterLARCD1007 116-117 M400-SY48 SylvesterLARCD1007 117-118 M400-SY49 SylvesterLARCD1007 120-121 M400-SY50 SylvesterLARCD1007 123-124 M400-SY51 SylvesterLARCD1007 129-130 M400-SY52 SylvesterLARCD1007 132-133 M400-SY53 SylvesterLARCD1007 133-134 M400-SY54 SylvesterLARCD1007 144-145 M400-SY55 Sylvester
M400-071 LNGT001 117.100 M400-LN01 Leviathan NorthM400-072 LNGT001 145.900 M400-LN03 Leviathan NorthM400-073 LNGT001 172.150 M400-LN06 Leviathan NorthM400-074 LNGT001 184.800 M400-LN07 Leviathan NorthM400-075 LNGT001 204.000 M400-LN08 Leviathan NorthM400-076 LNGT001 207.600 M400-LN09 Leviathan NorthM400-077 LNGT001 219.000 M400-LN11 Leviathan NorthM400-078 LNGT001 249.050 M400-LN13 Leviathan NorthM400-079 LNGT001 282.000 M400-LN15 Leviathan NorthM400-080 LNGT001 287.600 M400-LN16 Leviathan NorthM400-081 LNGT001 320.100 M400-LN17 Leviathan NorthM400-082 DUDH0130 129.800 M400-Dar004 CentenaryM400-083 DUDH0130 160.000 M400-Dar005 CentenaryM400-084 DUDH0131 211.000 M400-Dar011 CentenaryM400-085 DUDH0131 240.300 M400-Dar012 CentenaryM400-086 DUDH0131 300.000 M400-Dar013 CentenaryM400-087 MCD0362 850.900 M400-Dar015 CentenaryM400-088 MCD0362 910.900 M400-Dar021 CentenaryM400-089 MCD0362 1067.000 M400-Dar023 CentenaryM400-090 MCD0362 1183.110 M400-Dar025 CentenaryM400-091 MCD0424 247.000 M400-Dar029 CentenaryM400-092 MCD0424 261.000 M400-Dar030 CentenaryM400-093 MCD0424 286.450 M400-Dar032 CentenaryM400-094 MCD0424 320.200 M400-Dar033 CentenaryM400-095 MCD0424 386.000 M400-Dar034 CentenaryM400-096 MCD0424 450.100 M400-Dar036 CentenaryM400-097 MCD0424 555.000 M400-Dar038 CentenaryM400-098 MCD0393 193.700 M400-Dar041 CentenaryM400-099 MCD0393 204.600 M400-Dar042 CentenaryM400-100 MCD0393 246.000 M400-Dar043 CentenaryM400-101 MCD0393 330.100 M400-Dar047 CentenaryM400-102 MCD0393 352.300 M400-Dar048 CentenaryM400-103 MCD0393 377.800 M400-Dar050 CentenaryM400-104 MCD0393 407.100 M400-Dar051 CentenaryM400-105 MCD0393 558.700 M400-Dar053 CentenaryM400-106 MCD0428 358.500 M400-Dar056 CentenaryM400-107 MCD0428 374.700 M400-Dar057 CentenaryM400-108 MCD0428 389.800 M400-Dar058 CentenaryM400-109 MCD0428 440.550 M400-Dar059 CentenaryM400-110 MCD0428 452.000 M400-Dar060 CentenaryM400-111 MCD0428 690.800 M400-Dar061 CentenaryM400-112 CD10628 243.500 - ConquerorM400-113 CD10628 406.620 - ConquerorM400-114 CD10628 435.106 - ConquerorM400-115 CD10628 444.310 - Conqueror
M400-069
M400-070
A-61
M400-116 CD10628 460.085 - ConquerorM400-117 CD10628 464.182 - ConquerorM400-118 TD10887 198.400 - AthenaM400-119 TD10887 242.000 - AthenaM400-120 TD10887 315.700 - AthenaM400-121 TD10887 562.700 - AthenaM400-122 TD10229 117.300 - AthenaM400-123 TD10229 147.500 - AthenaM400-124 TD10229 184.500 - AthenaM400-125 TD10229 213.300 - AthenaM400-126 TD10229 219.500 - AthenaM400-127 BUGD049 182.76-182.81 - BullantM400-128 BUGD049 194.88-194.93 - BullantM400-129 CD10662 273.26-273.309 - MaximusM400-130 CD5026 164.500 - East RepulseM400-131 CD5026 175.400 - East RepulseM400-132 CD5026 197.900 - East Repulse
TD10465 120-121 - AthenaTD10465 150-151 (x2) - AthenaTD10269 161-162 - AthenaTD10269 168-169 - AthenaTD10269 174-175 - AthenaTD10465 109-110 - AthenaTD10465 154-155 - AthenaTD10269 129-130 - AthenaTD10269 138-139 - AthenaTD10269 144-145 - Athena
M400-135 GTD0025 88.45-88.5 - TrafalgarM400-136 GTD0025 168.13-163.18 - TrafalgarM400-137 GTD0025 168.3-168.35 - TrafalgarM400-138 GTD0025 170.13-170.18 - TrafalgarM400-139 HRD0026 139.33-139.38 - ChaffersM400-140 HRD0026 156.46-156.51 - ChaffersM400-141 HRD0026 208.09-208.14 - ChaffersM400-142 HRD0026 214.4-214.45 - ChaffersM400-143 HRD0026 248.31-248.36 - ChaffersM400-144 HRD0026 299.78-299.83 - ChaffersM400-145 HRD0026 317.72-317.77 - ChaffersM400-146 HRD0026 338.61-338.66 - ChaffersM400-147 HRD0026 359.03-359.08 - ChaffersM400-148 HRD0026 364.61-364.66 - Chaffers
2900147 28-30 - Trafalgar2900147 34-36 - Trafalgar2900147 42-44 - Trafalgar2900147 50-52 - Trafalgar2900147 58-60 - Trafalgar2900147 66-68 - Trafalgar2900147 72-74 - Trafalgar2900147 82-84 - Trafalgar2900147 86-88 - Trafalgar3800309 0-2 - Chaffers3800309 6m-8m - Chaffers3800309 18-20 - Chaffers3800309 24-26 - Chaffers3800309 28-30 - Chaffers3800309 30-32 - Chaffers
M400-133
M400-134
M400-149
M400-150
A-62
3800309 38-40 - Chaffers3800309 42-44 - Chaffers3800309 46-48 - Chaffers3800309 52-54 - Chaffers
WB0801CD 116.0m Wallaby DeepsWB0801CD 128.5m Wallaby DeepsWB0801CD 218.5m Wallaby DeepsWB0801CD 233.0m Wallaby DeepsWB0801CD 236.9m Wallaby DeepsWB0801CD 377.5m Wallaby DeepsWB0801CD 378.6m Wallaby DeepsWB0801CD 403.8m Wallaby DeepsWB0801CD 426.1m Wallaby DeepsWB0801CD 470.8m Wallaby DeepsWB0801CD 610.65m Wallaby DeepsWB0801CD 790.1m Wallaby DeepsWB0801CD 847.8m Wallaby DeepsWB0801CD 864.4m Wallaby DeepsWB0801CD 1141.1m Wallaby DeepsWB0801CD 1145.5m Wallaby DeepsWB0801CD 1175.1m Wallaby DeepsWB0801CD 1183.3m Wallaby DeepsWB0801CD 1193.9m Wallaby DeepsWB0801CD 1201.9m Wallaby DeepsPTS002 CD2427 486.6 St IvesPTS016 CD10662 272.3 St IvesPTS017 CD10662 375.5 St IvesPTS026 CD10662 202.91 St IvesPTS028 CD10662 377.8 St IvesPTS029 CD10662 700.6 St IvesPTS110 CD10662 80.4 St IvesPTS111 CD10662 111 St IvesPTS112 CD10662 134 St IvesPTS113 CD10662 827.95 St IvesPTS114 CD10662 925.1 St IvesPTS115 AU1-023 125.7 St IvesPTS116 AU1-023 128.3 St IvesPTS117 AU1-023 132.9 St IvesPTS118 AU1-023 134.2 St IvesPTS119 AU1-023 137 St IvesPTS120 AU1-023 139.8 St IvesPTS121 CD10662 568.5 St IvesPTS122 CD7069 352.2 St IvesPTS123 VU12-36 66.2 St Ives
A-63