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1994

Spatial variations in the thickness and coal qualityof the Sangatta Seam, Kutei Basin, Kalimantan,IndonesiaChairul NasUniversity of Wollongong

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Recommended CitationNas, Chairul, Spatial variations in the thickness and coal quality of the Sangatta Seam, Kutei Basin, Kalimantan, Indonesia, Doctor ofPhilosophy thesis, Department of Geology, University of Wollongong, 1994. http://ro.uow.edu.au/theses/1409

SPATIAL VARIATIONS IN THE THICKNESS AND COAL QUALITY OF THE SANGATTA SEAM, KUTEI BASIN, KALIMANTAN, INDONESIA

A thesis submitted in partial fulfilment of the requirements for the award of the degree of

DOCTOR OF PHILOSOPHY

from

THE UNIVERSITY OF WOLLONGONG NEW SOUTH WALES, AUSTRALIA

by

CHAIRUL NAS

(B.Sc (AGP Bandung), B.Sc.Hons (ITB), M.Sc)

DEPARTMENT OF GEOLOGY 1994

The contents of this thesis are the results of original research

by the author and material contained herein has not been

submitted to any other university or similar institution for a

higher degree .

ft—

CHAIRUL NAS

ACKNOWLEDGMENTS

As I complete this work I am grateful to God (Allah).

This study has been carried out since early 1989 under a bilateral cooperative agreement between the Australian and Indonesian governments who provided an A I D A B scholarship. I would like to express m y gratitude to the regional director of A I D A B (in Sydney) and his staff who have supported this program.

I would like to express my deep appreciation to my supervisors Associate Professor Brian Jones, Drs Adrian Hutton and Ernest Baafi for their advice. Associate Professor Brian Jones has encouraged and patiently guided this study through his broad knowledge on sedimentary depositional systems, statistics and computer programming. Dr Adrian Hutton supervised the coal geology and organic penological work, visited the field area and provided great assistance during the final stage of the thesis. Dr Ernest Baafi introduced the author to the concept and application of geostatistical techniques in coal and Fortran-77L computer programming.

I thank Associate Professor Tony Wright, Head of the Department of Geology of University of Wollongong, for providing the many facilities used in this study and Barbara McGoldrick for assistance in the use of the departmental facilities. I also thank Dr Alan Cook for his suggestions especially in the earliest stage of this study. Special thanks go to Avis Depers for his suggestions on coal penological techniques, M a x Perkins for computer services, Glen Martin for helping with X R D analysis, David Carie for making some thin sections and undertaking S E M and E D X analysis, and Suprapto and Nining Sudininingrum for their help with the trace element analysis in M T D C Chemical Lab, Bandung.

I am indebted to Drs Joan Esterle and Tim Moore for the help that I received from them. I have benefited from fruitful discussions, suggestions and comments on organic constituents of coal from Dr Joan Esterle. She also provided a number of wood and peat samples (in the form of polished blocks) to compare with the Sangatta coal macerals and supplied books, theses and papers related to this field. Dr Tim Moore provided suggestions on etching techniques and paid attention to this study through an intensive E-mail communication. His suggestions and comments on coal petrology were very valuable for this study. He also supplied the author with many papers. His wife, Dr Jane Shearer, sent fifteen diskettes of her P h D thesis to Wollongong. I am also thankful to Professor Claus Diessel for his suggestions and comments on the environment of deposition of the Sangatta seam, to Dr Chris Fielding for his critical comments on coal seam modelling and to and Dr Chris Fergusson for his suggestions on coal seam structures.

I express great appreciation to the management and geological staff of P.T Kaltim Prima Coal for providing many facilities during m y two periods of field work, for permission to use core samples and coal data files only available in the company. Steve McMillan (Chief of Mining Geology), Surya Putra (Senior Geologist) and Made (Computing Geologist) provided access and help with some computer drawing techniques. Steve McMillan also read and commented on parts of the thesis.

The management and exploration staff of P.T Batubara Bukit Asam, especially Yulizar (Manager of Mining) and Abdul Fatah (Chief of Exploration) are thanked for providing accommodation and a large set of Bukit Asam coal data during 1990 field trip to Bukit Asam.

I thank Dr Ukar Sulistijo (Director of Mineral Technology Development Centre, Bandung) for encouraging the author to take the opportunity of this study program and Dr Hikaman Manaf (Director of Manpower Development Centre for Mines, Bandung) for supporting this study.

During my study I also had the advantage of fruitful discussions with most sedimentology and coal postgraduate students in the Department of Geology, especially B Daulay, A Pujobroto, M Faiz, H Sutarwan, Y Kusumabrata, Surono and Herudiyanto. I also had help from Z Ichwan (Mining Engineering), Susilohadi and Jusmadi (Geology, U N S W ) who provided useful comments and suggestions about computer programming. Graham Ohmsen checked English expression in the earlier draft of some chapters. I would like to thank them for all this help.

Last, but not least, I am proud and thankful to my wife Novi and my son Meivi for their encouragement, understanding, attention and cooperation during the period of this study. To m y mother Rohana and m y parents in law M r and Mrs Bustanuddin, who allowed me to be away from them and always prayed for m y success, I am sincerely grateful.

ABSTRACT

The Sangatta coal seam, which contains high volatile bituminous coal and is the most important seam in the Sangatta Coalfield, was deposited within a Late Middle Miocene fluvial system that occupied the northern Kutei Basin, Indonesia. A study of clastic sedimentology, coal petrology of standard and etched coal samples, thickness and coal quality parameters, integrated with a geostatistical analysis, identified the depositional environment of the seam. This study indicates that the coal seam was deposited within the floodplain of a mixed-load fluvio-deltaic system with the rivers flowing southeastward. This sedimentary system is believed to have been a major control on the development of the Sangatta peat mire.

Local changes in sedimentary facies below and above the Sangatta seam caused variations in the local rates of subsidence and compaction which in turn controlled the peat swamp morphology and coalification pattern. The morphological variations governed hydrologic conditions in the swamp which, in turn, influenced peat accumulation and subsequent geological processes acting on, and within, the peat. These factors also influenced seam thickness, maceral composition and coal quality parameters.

The Sangatta seam has an average thickness of 6 m. The coals are characterised by a high vitrinite (average of 9 1 % ) , low liptinite (average of 3 % ) , low inertinite (average of 3 % ) , very low mineral matter (average of 2%) and low sulphur (average of 0.4%). The seam formed as a raised peat bog and, at some stages, was confined by river channels with vegetated levees. The general climate was very humid.

The Sangatta seam shows a bimodal normal thickness distribution with a high variability, a low degree of regularity (R = 0.36) and a low degree of spatial continuity, with a range of influence of 420 m. The seam formed under a complex process which involved an initial stage of peat generation followed by thickness modification attributed to geological process such as erosion (washout) and faulting. The spatial distribution of the thickness is anisotropic with the greatest continuity of thickness in a southeast direction (135°) which parallels the direction of clastic sedimentation in the coalfield. There is a negative statistical correlation between the local mean of the thickness and the thickness variability, whereby the thickest parts of the seam have a less variable thickness than the thinner parts.

The Sangatta seam was deposited in four geographic zones; the zones also correspond to differing geological processes within the zones. Within each zone the statistical parameters are zone specific. In the western zone the seam is thickest, does not split, has unimodal thickness and sulphur populations, the smallest thickness variability, greatest thickness continuity {range = 700 m ) , greatest thickness isotropy, abundant structured vitrinite, smallest number of clastic partings and a low ash content. The central zone has a bimodal population and a high variability for the thickness data, low thickness continuity (range = 300 m ) , low anisotropic thickness distribution, low sulphur content, little woody tissue and mostly degraded plant tissues. The eastern zone shows the greatest thickness variability with a relatively high ash yield, lowest thickness regularity (R = 0.23) and a strong thickness anisotropy. The northern zone has statistical parameters that tend to have intermediate values.

During peat accumulation the four zones had different depositional histories. The central zone formed as the central part of a raised bog, but immediately subsided, resulting in retardation of peat development. The western zone experienced the most stable

development pattern of any zone. In the eastern zone, although subsidence was not as great as in the central zone, syn-depositional structures and subsequent sedimentary processes acted on the coal seam. The northern zone is the least known part of the seam due to a limited drilling program, although preliminary data indicate it experienced a similar history to the eastern zone.

The depositional model formulated should improve the geological certainty in reserve estimation, mine planning and utilisation of the Sangatta coal. The zoned nature of the thickness and quality data necessitates "zoned kriging" for coal reserve estimation and in mine planning. In "zoned kriging", the depositional model for the Sangatta seam should control the steps in geostatistical reserve estimation. More specifically, reserve estimation should be undertaken separately for each zone.

This study can be used as a predictive model for coal exploration and basin analysis assessment in other Indonesian coalfields where geological conditions are similar.

TABLE OF CONTENTS

LIST OF FIGURES LIST OF TABLES LIST OF PLATES LIST OF APPENDICES

CHAPTER ONE - INTRODUCTION 1

1.1 THE STUDY AREA 1

1.2 PREVIOUS STUDIES 2

1.3 SCOPE AND METHOD OF RESEARCH 5

1.4 AIMS OF THE STUDY 6

CHAPTER TWO - GEOLOGY AND SEDIMENTATION 9

2.1 INTRODUCTION 9

2.2 REGIONAL GEOLOGY 9 2.2.1 General Geological Setting 9 2.2.2 Structural Pattern of the Kutei Basin 10 2.2.3 Sedimentation Pattern of the Kutei Basin 12

2.3 GEOLOGY OF THE SANGATTA COALFIELD 15 2.3.1 Structural Geology 15 2.3.2. Stratigraphy and Sedimentology 18 2.3.3 Environment of Deposition 22

CHAPTER THREE - SEDIMENTOLOGY OF CLASTIC INTERSEAM DEPOSITS . 25

3.1 INTRODUCTION 25

3.2 GENERAL DESCRIPTIONS 25

3.3 THICKNESS AND MAJOR LITHOLOGICAL VARIATIONS 27

3.4 FACIES DETAILS 31 3.4.1 Coarse-grained facies 31 3.4.2 Fine-grained facies 40 3.4.3 Lateral accretion 46 3.4.4 Facies relationships 48 3.4.5 Palaeocurrents 50 3.4.6 Syn-depositional Structures 51

3.5. DISCUSSION AND SUMMARY 54

CHAPTER FOUR - COAL SEAM GEOMETRY 57

4.1 INTRODUCTION 57

4.2 ADVANTAGE OF GEOPHYSICAL WELL-LOGS 58

4.3 CONTROL OF THE THICKNESS VARIABILITY 59

4.4 STRUCTURES IN THE SANGATTA SEAM 63

4.5 FLOOR AND ROOF STRATA AND PARTINGS 64

4.6 SEAM QUALITY DATA 69

4.7 COAL SEAM DEPOSITIONAL MODEL (CONCLUSIONS) 73

CHAPTER FTVE - COAL PETROLOGY 75

5.1 INTRODUCTION 75

5.2 COAL PETROLOGY TECHNIQUES 76

5.3 COAL FACIES AND THE DEPOSITIONAL ENVIRONMENTS 77

5.4 MACERAL COMPOSITION OF THE SANGATTA SEAMS 80

5.5 MINERAL AND TRACE ELEMENTS IN THE SANGATTA SEAM 91

5.6 PETROGRAPHIC ANALYSIS OF ETCHED COAL SAMPLES . 94

5.7 LATERAL PETROLOGICAL VARIATIONS OF THE SANGATTA SEAM 100

5.8 VERTICAL VARIATIONS IN LITHOTYPES 102

5.9 VrrRINITE REFLECTANCE OF THE SANGATTA SEAM 104

5.10 DISCUSSION AND SUMMARY 107

CHAPTER SK - STATISTICAL PARAMETERS OF THE SANGATTA SEAM 117

6.1 INTRODUCTION 117

6.2 DATA COLLECTION AND PREPARATION 118

6.3 STATISTICAL METHODS 119 6.3.1 Basic Statistics 119 6.3.2 Spatial Statistics 121

6.4 RESULTS OF THE STATISTICAL ANALYSIS 134

6.4.2 Ash content 6.4.3 Sulphur Content 143 6.4.4 Air Dried Moisture Content 146 6.4.5 Calorific Value and Volatile Matter 147 6.4.6 Ash composition 150 6.4.7 Ultimate Analysis Data 152 6.4.8 Types of Sulphur 153 6.4.9 Multivariate Features of Coal Data 154

6.5 SUMMARY 155

CHAPTER SEVEN - DEPOSITIONAL ENVIRONMENT OF THE SANGATTA SEAM 159

7.1 INTRODUCTION 159

7.2 TECTONIC AND SEDIMENTARY CHARACTERISTICS OF THE KUTEI BASIN 159

7.3 SEAM DEVELOPMENT 161

7.4 DEPOSITIONAL PARAMETERS OF THE SANGATTA SEAM 163 7.4.1 Clastic interseam strata 163 7.4.2 The Sangatta Seam 166

7.5 DEPOSITIONAL HISTORY OF THE SANGATTA SEAM 172

CHAPTER EIGHT - FACTORS GOVERNING RESERVE ESTIMATION . 195

8.1 CONCEPTS IN RESERVE ESTIMATION 195

8.2 FACTORS IN COAL RESERVE ESTIMATION 196

8.3 DEPOSITIONAL MODELS IN COAL RESERVE ASSESSMENT 198

8.4 REVIEW OF RESERVE ESTIMATION IN THE SANGATTA COALFIELD 203

8.5 PROPOSED COAL ESTIMATION METHODS 207

CHAPTER NINE - CONCLUSIONS 209

9.1 CONCLUSIONS 210

9.2 FURTHER WORK AND RECOMMENDATIONS 216

REFERENCES 219

LIST OF FIGURES

Figure 1.1 Location map of the study area 240 Figure 1.2 Coal mining carried out in seven open pit mines 241 Figure 1.3 Distribution of coal seams in seven open pit mines 242 Figure 1.4 Flow chart of aspects and procedures in this study 243

Figure 2.1 Distribution of coal deposits in eastern Kalimantan 244 Figure 2.2 Major structural elements in eastern Kalimantan 245 Figure 2.3 Trend of major fold axes in the Kutei Basin 246 Figure 2.4 Hypothetical model for structural development, 247

central part of Kutei Basin Figure 2.5 The development of sedimentation pattern during 248

Early to Late Miocene in the Kutei Basin Figure 2.6 Redefined stratigraphic succession of the Kutei Basin 249 Figure 2.7 Geological map of the Sangatta Coalfield 250 Figure 2.8 Stratigraphy of the Sangatta Coalfield 251

Figure 3.1 Situation of the Sangatta Coalfield 252 Figure 3.2 Locations of cored drillholes in the Sangatta Coalfield 253 Figure 3.3 Diagrammatic section of the stratigraphy 254

of the Sangatta Coalfield Figure 3.4 Idealised geological cross-section of 255

Melawan-Sangatta area Figure 3.5 W - E seam and lithologic correlation of boreholes 256 Figure 3.6 S W - N E seam and lithologic correlation of boreholes 258 Figure 3.7 Drillhole locations of correlated sections 260 Figure 3.8 Isopach and first order trend surface maps 261

of the Sangatta-B2 clastic interval Figure 3.9 Lithologic and geophysical logs of drillhole C3486 262 Figure 3.10 Isopach, trend surface and residual maps 263

of Sangatta-Middle clastic interval Figure 3.11 Structure contour, trend surface and 264

residual maps of top of the Sangatta seam Figure 3.12 Sand percentage, first order trend surface 265

and residual maps of the Sangatta-Middle clastic interval Figure 3.13 Isopach, first order trend surface and 266

residual maps of the Sangatta-Pinang clastic interval Figure 3.14 Sand percentage, first order and residual 267

maps of the Sangatta-Pinang clastic interval Figure 3.15 Outcrop photos from the Sangatta Coalfield 268 Figure 3.16 Correlation of some measured sections 270 Figure 3.17 Facies relationships in the clastic interval 271

above Middle seam Figure 3.18 Facies relationships of clastic sediments 273

near the Hatari, E-West and R O M road junction Figure 3.19 Models for fining-upward sequences 276

Figure 3.20 Outcrop photos from the Sangatta Coalfield 277 Figure 3.21 Lithologic section from drill core F5253 (Hatari Pit) 279 Figure 3.22 Lithologic section from drill core F5304 (E-West Pit) 282 Figure 3.23 Facies relationships of the Middle seam 284 Figure 3.24 Measured sections in MS-8 and MS-5 286 Figure 3.25 Schematic facies relationships of sedimentary strata 287 Figure 3.26 Typical diffractogram of clay mineral 288 Figure 3.27 Contour maps of B 2 seam thickness 289 Figure 3.28 Contour map of ash yield and sulphur content 290

of the B 2 seam Figure 3.29 Profiles of ash yield and sulphur content of the B 2 seam 291 Figure 3.30 Palaeocurrent directions in the Sangatta Coalfield 292 Figure 3.31 Grand mean of palaeocurrent data 293 Figure 3.32 Compaction of peat to coal in CN-1 (C-North Pit) 294 Figure 3.33 Photomicrographs of sedimentary rocks 295 Figure 3.34 Growth fault in the Hatari Pit 297

Figure 4.1 Gamma ray and density logs used in coal seam modelling 298 Figure 4.2 Specific gravity and ash yield, Sangatta coal samples 300 Figure 4.3 The Sangatta seam model 1 301 Figure 4.4 The Sangatta seam model 2 302 Figure 4.5 Detailed correlation of the Sangatta seam 303

in the eastern part of the Sangatta Coalfield Figure 4.6 Exposures of the Sangatta seam in the Sangatta Coalfield 304 Figure 4.7 Structural contours of the top of the Sangatta coal seam 305 Figure 4.8 Schematic cross-sectional model of 306

the Sangatta-Middle split system Figure 4.9 Three models on vertical variation of sulphur 307

contents in the Sangatta seam Figure 4.10 Typical vertical variation of sulphur contents in 308

low sulphur coals from the Sangatta seam Figure 4.11 Typical vertical variation of sulphur contents in 309

moderately high low sulphur coals from the Sangatta seam Figure 4.12 Typical vertical variation of sulphur contents 310

in high sulphur coals from the Sangatta seam Figure 4.13 Typical vertical variation of volatile matter 311

content and calorific values in the Sangatta seam

Figure 5.1 Coal sample preparation for petrographic analysis 312 Figure 5.2 Procedure in etching coal samples 313 Figure 5.3 Petrographic composition of the Sangatta coal 314 Figure 5.4 Histogram and probability graph of vitrinite content 315 Figure 5.5 Composition of the vitrinite macerals 316 Figure 5.6 Percentage distributions of three sub-macerals of vitrinite 317 Figure 5.7 Dendogram of petrographic data from the Sangatta seam 318 Figure 5.8 Percentages of vitrinite macerals from etched samples 319 Figure 5.9 Vitrinite and liptinite contents in the Sangatta seam 320 Figure 5.10 Telovitrinite and telinite contents from etched samples 321

Figure 5.11 Detrovitrinite and vitrodetrinite contents 322 from etched samples

Figure 5.12 Cork tissue derived vitrinite and phylovitrinite 323 contents from etched samples

Figure 5.13 Telovitrinite content from unetched samples 324 and angiosperm derived telinite content from etched samples

Figure 5.14 Lithotype profile of the Sangatta seam in Drill hole F5304 325 Figure 5.15 Vertical variation in petrographic composition 326

from unetched samples, Sangatta seam in Drill hole C3536 Figure 5.16 Vertical variation in petrographic composition 327

from unetched samples, Sangatta coal in mine face HT-3,

Hatari Pit Figure 5.17 Plot of the Sangatta coal rank data in Teichmuller 328

and Teichmuller's coalification diagram Figure 5.18 Vitrinite reflectance and coefficient of variation 329

for the vitrinite reflectance Sangatta seam Figure 5.19 Plots of the Sangatta petrographic data on 330

Diessel's TPI-GI diagram Figure 5.20 Distribution of woody tissue derived vitrinite and 331

detrovitrinite in the Sangatta coal seam Figure 5.21 Distribution of inferred precursor plants of 332

vitrinite macerals in the Sangatta coal seam

Figure 6.1 Location map of boreholes intersecting the Sangatta seam 345 Figure 6.2 X-Y plots for Q-mode cluster analysis 346 Figure 6.3 Distribution of sample locations of each clustered group 347

(from 6 variables), the Sangatta seam Figure 6.4 Distribution of sample locations of each clustered group 347

(from 5 variables), the Sangatta seam Figure 6.5 Theoretical spherical model of variogram (x-y plot) 348 Figure 6.6 Histograms for combination and core hole thickness data 350 Figure 6.7 Isopach map of the Sangatta seam 351 Figure 6.8 Moving average and coefficient of variation 352

maps of thickness Figure 6.9 Third order trend surface and residual maps of thickness 353 Figure 6.10 Third order trend surface and residual maps of 354

thickness in the southern area Figure 6.11 First order trend surface and residual maps of 355

thickness in the southern area Figure 6.12 Local means vs coefficient of variations and 356

local means vs standard deviations, Sangatta seam thickness Figure 6.13 Omnidirectional variogram of all thickness data 357 Figure 6.14 H-scattergram of thickness data 358 Figure 6.15 Directional variograms of the thickness data, 359

Sangatta seam Figure 6.16 Directional variogram from randomised thickness data 361 Figure 6.17 Histogram and probability graph of ash yield 362

from composite sample, Sangatta seam

Figure 6.18 Histogram and probability graph of ash yield 363 from ply samples, Sangatta seam

Figure 6.19 Plot of ply and composite samples ash yields, 364 Sangatta seam

Figure 6.20 M a p of ash yield from ply samples, Sangatta seam 365 Figure 6.21 First order trend surface and residual maps of 366

ash yield from ply samples, Sangatta seam Figure 6.22 Moving average and coefficient of variation maps of 367

ash yield from ply samples, Sangatta seam Figure 6.23 Scatterplots local means vs standard deviations 368

and local means vs coefficients of variations of ply sample ash yield

Figure 6.24 Contour maps of composite and ply samples ash yield 369 Figure 6.25 Omnidirectional variograms of original and 370

the smoothed ash yield data Figure 6.26 Four directional variograms of the smoothed 371

ash yield data Figure 6.27 Histograms of sulphur data from composite and 372

ply samples Figure 6.28 Correlation between ply and composite samples 373

sulphur data Figure 6.29 Spatial distribution composite samples sulphur data 374 Figure 6.30 First order trend surface and residual maps of 375

sulphur data Figure 6.31 Fourth order trend surface and residual maps of 376

sulphur data Figure 6.32 Moving average and coefficient of variation maps 377

of sulphur Figure 6.33 Omnidirectional experimental and spherical modelled 378

variograms of sulphur data Figure 6.34 Four directional experimental variograms of 379

sulphur data Figure 6.35 Histogram and statistical parameters of moisture 380

content data Figure 6.36 Contour and moving average maps of moisture 381

content data Figure 6.37 First and third order trend surface maps, 382

moisture content Figure 6.38 Omnidirectional and directional variograms of 383

moisture content data Figure 6.39 Histogram of calorific value data, Sangatta seam 384 Figure 6.40 Contour and moving average map of calorific value 385 Figure 6.41 First and second order trend surface maps of 386

calorific values Figure 6.42 Omnidirectional and directional variograms of 387

calorific values Figure 6.43 Histogram of volatile matter content data 388 Figure 6.44 Contour and moving average maps of volatile 389

matter content

Figure 6.45 First and second order trend surface maps of 389 volatile matter content

Figure 6.45 First order trend analysis of volatile matter data 390 Figure 6.46 Omnidirectional and directional variograms of 391

volatile matter content Figure 6.47 Delta volatile matter content map 392 Figure 6.48 R-mode cluster analysis of chemical data of the 393

Sangatta seam Figure 6.49 Contour and moving average maps of silicate and 394

clay mineral derived elements in coal ash, the Sangatta seam Figure 6.50 First and second order trend surface maps of 395

silicate and clay mineral derive elements in coal ash, the Sangatta seam

Figure 6.51 Contour and moving average maps of Si/Al ratio in 396 coal ash of the Sangatta seam

Figure 6.52 Contour, moving average and trend surface maps of 397 carbonate and sulphate mineral derived elements in coal ash, the Sangatta seam

Figure 6.53 Contour map and moving average maps of M g O content 398 in coal ash of the Sangatta seam

Figure 6.54 Contour and moving average maps of C a O + M g O content 399 in coal ash of the Sangatta seam

Figure 6.55 M a p of Nitrogen content in the Sangatta seam 400 Figure 6.56 Correlation between organic and inorganic sulphur 401

of the Sangatta seam Figure 6.57 M a p of organic/inorganic ratio of sulphur content 402

in the Sangatta seam Figure 6.58 Statistical summary of the thickness data 403 Figure 6.59 Variations in statistical population and vertical 404

development of sulphur content

Figure 7.1 Distribution of the Sangatta coal seam and the 405 four spatial zones, Sangatta Coalfield

Figure 7.2 Hypothetical model for the development of the 406 Okavango River, Bostwana Africa

Figure 7.3 Block diagram of the relationship between the 407 Sangatta peat swamp and clastic environments

Figure 7.4 Summary of coal seam characteristics in the 408 four zones of the Sangatta seam

Figure 7.5 Cross-section of coal seam characteristics summary 409 in the four zones of the Sangatta seam

Figure 7.6 Depositional models of the Sangatta peat swamp 410 Figure 7.7 Comparison between geological conditions in the 411

Bukit Asam Coalfield and the Sangatta Coalfield Figure 7.8 Statistical summary of the thickness data from the 412

Sangatta seam and Bukit Asam Al seam Figure 7.9 Tabulated summary showing different geological 413

conditions and interpreted peat development systems between the Sangatta and Al seams

Figure 7.10 Raised bog model for the thick coal seams in the 414 Powder River Basin (U.S.A)

Figure 7.11 Hypothetical model for the lower bench of the 414 Upper Hence seam, Kentucky (U.S.A)

Figure 8.1 USGS coal reserve classification system 415 Figure 8.2 Characterisation of coal resources 416 Figure 8.3 Coal reserves distinguished from three main factors 417 Figure 8.4 Australian coal reserves classification system 418

LIST O F T A B L E S

Table 2.1 Stratigraphy of the Kutei Basin 419 Table 2.2 Stratigraphy of the Mahakam Coalfield, central Kutei Basin 420

Table 3.1 Petrologic composition from some sandstone samples 421

Table 5.1 AS 2856-1986 coal maceral classification system 422 Table 5.2 Petrographic data of the Sangatta coal samples 423 Table 5.3 Petrographic data of bench samples from the 425

Sangatta seam and composite samples from the B2, Middle and Pinang seams

Table 5.4 Vitrinite maceral compositions in etched samples 426 Table 5.5 Trace elements in the Sangatta coal 427

Table 6.1 Summary of basic statistical parameters 428 Table 6.2 Some statistical formula 429 Table 6.3 Statistical elements of Q-mode clustered group 430 Table 6.4 Statistical elements of Q-mode clustered group 431 Table 6.5 Parameters of variograms 432 Table 6.6 Summary of fit (R) and significance (F) tests, 433

trend surface analysis

LIST O F P L A T E S

Plate 5.1 Photomicrographs of coal from standard petrography 333 Plate 5.2 Photomicrographs of coal from standard petrography 335 Plate 5.3 Photomicrographs of coal from standard petrography 337 Plate 5.4 Photomicrographs of coal from standard petrography 339 Plate 5.5 Photomicrographs of coal from etched samples 341 Plate 5.6 Structures in the Sangatta coal and modern plants 343

LIST OF APPENDICES

Appendix 3.1 Gamma-ray logs from some drill holes showing variations of fining-upward sequences in the Sangatta Coalfield.

Appendix 3.2 Lithological logs from some drill holes showing vertical variations of lithology in the Sangatta Coalfield.

Appendix 3.3 Combination of lithological and geophysical logs from some drill holes showing variations of lithology and the vertical development, Sangatta Coalfield.

Appendix 3.4 Palaeocurrent measurements and the correction for tectonic tilt, Sangatta Coalfield.

Appendix 3.5 Thickness data for the Sangatta - Middle interseam deposits.

Appendix 3.6 Thickness data for the Sangatta - Pinang interseam deposits.

Appendix 3.7 Sand percentage data for the Sangatta - Middle and Sangatta - Pinang interseam deposits.

Appendix 3.8 Thickness and coal quality data for the B2 seam.

Appendix 6.1 Computer program (Fortran-77L) LIMIT.

Appendix 6.2 Computer program (Fortran-77L) WIND.

Appendix 6.3 Computer program (Fortran-77L) TREND.

Appendix 6.4 Computer program (Fortran-77L) RANDOM.

Appendix 6.5 Drill hole data for the Sangatta seam.

Appendix 6.6 • Cored hole data for the Sangatta seam.

Appendix 6.7 Ply samples data for the Sangatta seam.

Appendix 6.8 Ash composition and ultimate analytical data for the Sangatta seam.

Appendix 7.1 Drill hole data for the Al seam, Bukit Asam Coalfield.

Appendix 8.1 "ZONED KRIGING" procedure in coal reserve assessment.

CHAPTER ONE

INTRODUCTION

1.1 THE STUDY AREA

The study is concentrated in the Sangatta Coalfield, Kalimantan, Indonesia, which has

a good potential for coal production. As this coalfield has already been explored in

detail, it has a good base of coal data for coal geological studies. The Sangatta

seam, the most important seam in the area, has the largest volume of documented

geological information in the coal data base. Any models resulting from this study

can hopefully be applied to other seams in this coalfield and to other coalfields in

Indonesia, at least in those basins which have similar geological conditions.

With an area of approximately 60 km2, the study area is located between the

Sangatta and Bengalon Rivers in the eastern part of Kalimantan and is included in

the Bontang Sub-district, Kutei District, East Kalimantan Province of Indonesia with

Samarinda as the provincial capital. It is situated approximately 200 km northeast of

the oil city of Balikpapan (Fig. 1.1). Geographically the study area is located

between 117°27'E - 117°31'E and 0°33'N - 0°39'N. The temperature is very high

almost all the year.

The Sangatta Coalfield can be accessed by land, sea and air transport. Roads permit

access by any type of car (but preferably 4WD) to and from Samarinda via Bontang.

Small ships, to and from Samarinda, are also available for public transportation.

Helicopters and small 20 seat twin-engined CASA aircraft are operated to and from

Balikpapan or Samarinda on a daily basis by the coal company.

2

At an early stage of the exploration work, an extensive network of timber roads

provided numerous geological outcrops. The roads were also utilised by the

company's geologists to access natural coal outcrops.

The topography of the area is hilly and irregular (0 to 300 m above sea level), and

covered by regenerated rain forest. The Kutei National Park is a rain forest park

located southwest of the coalfield, along the south margin of the Sangatta River.

Geologically the Sangatta Coalfield is situated in the northern part of the Kutei

Basin. The Sangatta seam is the major seam in the Sangatta Coal Measures which

are located in the upper part of the Balikpapan Formation (Middle-Late Miocene).

The geology of the study area is described in Chapter 2.

This coal area has been developed by P.T. Kaltim Prima Coal (KPC) which is a

joint venture company comprising C R A (Australia) and B P (UK). This company has

been exploring, developing and exploiting the Sangatta coal under the production

sharing contract with the Indonesian State Coal Company, Perum Tambang Batubara.

At present, mining is carried out in 7 open pits (Fig. 1.2) with a target for an

optimal production rate of 7 million tonnes per year. The Sangatta seam, as the

major seam in the coalfield, occurs in 4 of the 7 pits (Fig. 1.3). The majority of the

run-of-mine coal is low in ash yield and sulphur content, and therefore no washery is

needed.

1.2 PREVIOUS STUDIES

According to an unpublished report written by Gunawan (1979), the earliest coal

3

geological work in the Sangatta Coalfield was by Ubagh (1934). Several thick, high-

quality seams were found during his work. However, the results of Ubagh's work

was not recognised by subsequent coal geological investigations due to the lack of a

retrievable filing system.

In 1976, when Rio Tinto Indonesia (RTI) and BP (UK) had an agreement to study

Indonesian coal deposits, these companies commenced an extensive literature search

on Kalimantan coal deposits (including old reports produced by Dutch geologists).

RTI sent one of its geologist to the area in 1978 to confirm Ubagh's report. The

result of this preliminary observation and confirmation was documented in an

unpublished company report (Putra, 1978).

Several geological studies carried out by Pertamina (the state-owned Indonesian oil

exploration company) and the Geological Survey of Indonesia (Sikumbang et al,

1981) included the Sangatta Coalfield as part of their survey and provided general

comments on mineral, coal and hydrocarbon potential, but did not consider the

Sangatta area as a prospective coal deposit. This was possibly because of the scale

and objectives of the survey which were of a regional type and did not concentrate

on coal deposits.

Based on the observations and coal samples collected from a number of outcrops by

the RTI geologist (Putra, 1978), the Sangatta area was thought to contain a number

of thick, high-quality seams. Afterwards the company decided this area was one of

the most attractive coal deposits in Kalimantan.

Based on this decision, the company included the Sangatta area in its exploration

4

concession when it commenced an exploration program in eastern Kalimantan. In

1982, RTI (later called CRA) and BP (UK) formed a new joint venture company

named Kaltim Prima Coal (KPC) and it was selected as one of contractors of the

Indonesian State Coal Company (Perum Batubara) during the national coal

development program. One of the objectives of the Kalimantan coal exploration

activities of KPC was to explore for open-cut deposits of export quality steaming

coal (Leeuwen and Muggeridge, 1986). The Sangatta Coalfield is one of the most

important targets that was investigated by KPC during its exploration period in terms

of in-situ coal reserves and their economic viability.

A systematic study of coal seam geology in the Sangatta Coalfield was undertaken

when detailed exploration was commenced by KPC in 1983. The major part of this

exploration program included detailed geological and topographic mapping, shallow

drilling with geophysical logging and extensive outcrop sampling of coal; the project

was completed in 1987. Seam thickness data were obtained from the combination of

lithological and geophysical logs. Quality data were obtained by sampling the seams

through outcrops and drill hole cores and cuttings. The results of this detailed

exploration program indicated that the Sangatta seam was the most persistent seam in

the Sangatta Coalfield (Leeuwen and Muggeridge, 1986).

A comprehensive geological report written by Muggeridge (1987) documented the

results of KPC's exploration work. Although this report was written in an academic

format, many of the well-documented exploration data were still not utilised

adequately. For example, many of the thickness and quality variations of seams

were stated unsystematically in a qualitative manner although a massive set of coal

thickness and quality data were available. Moreover, sedimentology which is a

5

major aspect in coal geological research, was not mentioned much in the report even

though the company had produced numerous measured sections from outcrops and

drill holes from initial exploration work.

The geological information has continuously accumulated since the mine development

started at the end of 1987. During the construction phase, more wells were drilled

and more outcrops created. With respect to this mass of geological data, integrated

research was carried out to study some geological aspects of the Sangatta seam in

the area. This study utilised the existing coal thickness and quality data, lithological

and geophysical logs, core and outcrop samples and field sedimentological work.

Similar studies elsewhere have been beneficial in improving the understanding of coal

seam behaviour in several coalfields (e.g. Home et al., 1979; Ferm and Staub, 1984;

McCabe, 1984, 1987; Esterle and Ferm, 1986; Diessel, 1992). However, integrated

qualitative and quantitative studies on coal seam geological research involving

thickness, sedimentology, chemical and penological data are still rare.

The net result of the exploration programs that centred on Sangatta, is a mass of

data awaiting interpretation.

1.3 SCOPE AND METHOD OF RESEARCH

Coal reserve estimations are related to the spatial aspects of thickness and quality

parameters of the seam. Therefore, any improvement in the geological knowledge of

these parameters will be of particular benefit. For example, the understanding of the

depositional environments provides a better vision of the geometry and quality

distribution of seams.

6

The spatial variations of thickness and quality parameters of the Sangatta seam have

been characterised by studying the sedimentology of associated rocks, and the

chemical and petrographical properties of the coal seam. For the large data sets

(especially the thickness and quality data) to provide meaningful geological

information, they require statistical analysis. Therefore, an integrated approach

comprising geological and statistical (qualitative and quantitative) analyses was

applied in this study. The method included analyses of geological maps, measured

sections, lithologs, geophysical logs, outcrop features and coal petrology.

Quantitative analysis, consisting of basic and spatial statistics, involved thickness and

coal quality data from proximate and ultimate chemical analyses. Data and material

for this study were supplied from numerous drill holes and outcrops. The procedure

of this research is outlined in Figure 1.4.

1.4 AIMS OF THE STUDY

The major objectives of this study are:

1. to interpret the depositional environments of the Sangatta seam;

2. to discuss the use of the depositional model in coal geological

assessments, such as in basin analysis and in predicting thickness and

quality of coal seams;

3. to discuss the significance of the depositional model in reserve

classification and estimation systems, mine planning and coal utilisation;

and

4. to contribute to the study of depositional systems and reserve

classification and estimation of coal deposits.

7

These objectives are achieved by studying:

1. aspects of the sedimentology of interseam strata;

2. aspects of the coal seam geometry;

3. aspects of coal petrology; and

4. aspects of statistical variations in coal thickness and quality data.

8

9

CHAPTER TWO

GEOLOGY AND SEDIMENTATION

2.1 INTRODUCTION

This chapter describes the general geology and sedimentation pattern of the study

area. The description, commencing with the regional geology, followed by the local

geology, summarises the geological development of the study area in the context of

the development of the Kutei Basin. The geological development of the study area

is focused mainly on the depositional environment of the Balikpapan Formation, in

which the Sangatta seam was deposited.

2.2 REGIONAL GEOLOGY

2.2.1 General Geological Setting.

On the island of Kalimantan, the majority of coal deposits are distributed along the

eastern margin of the island, that is, from Bulungan Regency, in the north, to Pulau

Laut and Kintap in the south (Fig. 2.1). The coal was deposited within four Tertiary

sedimentary basins; Tarakan, Kutei, Asem Asem and Barito Basins (Samuel and

Muchsin, 1976; Koesoemadinata et ah, 1978).

In the early stage of their formation (Early Tertiary), these four basins formed a

single large basin, called the Eastern Kalimantan Basin, which occupied the eastern

part of Kalimantan (Samuel and Muchsin, 1976; Rose and Hartono, 1978; Pieters et

10

al., 1987; Umar et al, 1987). The basin is categorised as a cratonic (back-arc) basin

of the northwest Borneo subduction system (Hamilton, 1979; Land and Jones, 1987).

Van de Weerd and Armin (1992) suggested that a flexural down-warping of the

basement initiated the formation of the large Eastern Kalimantan Basin. After the

Tertiary rifting of the Makassar Strait, uplift of the Kuching and Meratus Highs

started to separate the Eastern Kalimantan Basin into four basins; Tarakan, Kutei,

Asem Asem and Barito Basins (Samuel and Muchsin, 1976; Sikumbang, 1986). The

uplift also caused a tectonic inversion in the Kutei Basin during the Early Miocene

causing a west to east sedimentation direction (Hamilton, 1979; Daly et al, 1987;

Wain and Berod, 1989).

2.2.2 Structural Pattern of the Kutei Basin

The Kutei Basin is located between the Kuching High in the west and the Makassar

Strait in the east. The basin is also bordered by the Mangkalihat Ridge in the north

and by the Paternoster Fault and Meratus Range in the south. Figure 2.2 shows the

major structural elements of eastern Kalimantan showing the position of the Kutei

Basin.

The geological structures of the Kutei Basin are dominated by folds, normal faults

and thrust faults. The trend of the major fold axes and the associated thrust faults,

in general, is north-northeast to south-southwest subparallel to the eastern coast of

Kalimantan (Fig. 2.3). The folds commonly have formed narrow anticlines separated

by flat synclines. The dips of strata tend to increase with the stratigraphic position

within the anticlines, that is, the older units have greater dips (Hamilton, 1979;

Gunawan, 1979).

11

The Samarinda Anticlinorium, the most intense and densely folded area in the Kutei

Basin, has tight folds and thrust faults (Samuel and Muchsin, 1976; Koesoemadinata

et al, 1978; Nas and Indratno, 1979; Land and Jones, 1987; Ott, 1987). Some mud

volcanoes and diapiric intrusion breccias were reported in this area by Land and

Jones (1987). From the Samarinda area the density and intensity of folds decrease

both westward and eastward.

The deformation in the Kutei Basin may have been initiated by the uplift of the

Kuching High and the rifting of the Makassar Strait (Hamilton, 1979; Daly et al,

1987; Wain and Berod, 1989). Based on the major structural characteristics, it is

believed that the deformation was mainly caused by a gravitational slumping system

(Koesoemadinata et al; 1978; Hamilton, 1979; Ott, 1987; van de Weerd and Armin,

1992) where the thick sediments in the Kutei Basin slid toward the rifted Makassar

Strait causing folding and thrusting in the strata (Fig. 2.4). This process may also

have produced overpressured shales in the lower part of the sedimentary fill which in

turn produced diapiric intrusions in the cores of anticlines.

The structural pattern of the Kutei Basin changes markedly to the north of the

Sangatta River (Muggeridge, 1987). This area is in a transitional zone between the

Kutei Basin and the Mangkalihat Ridge (Sikumbang et al, 1981). Folds typically

display gently dipping limbs with doubly plunging anticlines (e.g. Pinang Dome).

This may indicate that in the northern area deformation was less intensive.

The structural features, to some extent, are significant for defining the sedimentation

and seam distribution in the Kutei Basin. Tectonic events have controlled the

provenance and sedimentation pattern in the basin. The tectonic inversion in the

12

Kutei Basin has established a source area in the west (granitic, metamorphic rocks

and older Tertiary sediments) and a west to east sedimentation direction in the basin

during the Late Tertiary. Major seams in the Kutei Basin were deposited mostly on

fluvio-deltaic plains prograding eastward over the eastern part of Kalimantan and are

associated with Neogene terrestrial clastic sediments.

Gravitational slumping has formed significant structural features in the sedimentary

strata, including coal seams. Tight anticlines and flat synclines imply that coal

deposits within synclines have better techno-economic value than those within

anticlines. As the intensity of deformation decreases to the north, seams become

more workable for open cut mines especially within the syncline areas.

2.2.3 Sedimentation Pattern of the Kutei Basin

The Kutei Basin, covering some 60000 km2 (Land and Jones, 1987), contains a thick

sequence of sedimentary rocks with the maximum thickness up to 12200 m in its

depocentre (Rose and Hartono, 1978). In general, this sequence can be grouped into

Paleogene transgressive (the Kuaro, Telaki and Tuju Formations) and Neogene

regressive (the Pemaluan, Pulubalang, Balikpapan and Kampungbaru Formations) sub

sequences (Table 2.1). In the Mahakam area and south and west Samarinda areas,

Land and Jones (1987) proposed the following new names for formations of the

Neogene sedimentary strata - the Loa Duri, Loa Kulu, Parangat and Kamboja

Formations (from bottom to top). Correlation of each formation with the existing

Neogene formations is given in Table 2.2.

At present, the distribution of sedimentary units in the Kutei Basin is generally

13

controlled by the major north-northeast-trending folds where older Tertiary units are

commonly exposed in the cores of anticlines. The distribution of these units was

also initially controlled by the basin development during the Tertiary where the older

units are only exposed along the western margin of the basin. Eastward progradation

of the Mahakam Delta has been a major sedimentary process during the Neogene and

this has resulted in progressive lateral and vertical changes in sedimentary facies

from the west to the east. Laterally, sedimentary facies have changed progressively

from terrestrial sediments in the west into marine sediments in the east (Fig. 2.5).

Chronologically, in these regressive strata, the western sedimentary units are, in

general, older than the eastern units.

In the prograding delta sequence, lateral changes of sedimentological facies are more

readily recognised than vertical changes. This was caused by the presence of

numerous depositional environments in a particular period of time which led Marks

et al. (1982) to redefine the Neogene stratigraphic nomenclature of the Kutei Basin

(Fig. 2.6). In any particular area, several depositional environments ranging from

fluviatile to upper and lower delta plain and carbonate shelf are likely to be found.

Gunawan (1979) and Wain and Berod (1990) believed that several individual deltas

were active along the ancient Kutei coastline during the Late Tertiary. Consequently,

the sedimentary depositional system in northeastern part of the basin, that is, the

Sangatta area, was rather different from that in the central area. Their interpretation

was based on the southeastward directions of sedimentation in the Sangatta area

(Pattinama and Djunaedi, 1977) indicating that the sediments were not transported

from the Mahakam River. In the Sangatta oilfield, Pattinama and Djunaedi (1977)

even postulated an independent deltaic system with the river flowing from northwest

14

to southeast.

Although seams also occur in the Paleogene Kuaro Formation, most of the significant

seams were deposited in the Neogene regressive sub-sequence, that is, in the

Pemaluan, Pulubalang, Balikpapan and Kampungbaru Formations. The coal deposits

represent an integral part of the sedimentation package within the continually

prograding delta system as it moved eastwards. The area of maximum sediment

thickness, the depocentre, shifted progressively eastward with time (Fig. 2.5).

The general patterns and characteristics of seams in the Kutei Basin mentioned by

Koesoemadinata et al. (1978), and based on data mostly from the Mahakam area,

are:

seams were deposited on a terrestrial deltaic plain;

seams occur in most of the Tertiary sequences;

seams are laterally extensive;

seam are generally thin;

seams are numerous;

growth faults localise thick coal; and

there is a large coal potential.

Most of these characteristics were supported by Land and Jones (1987). They added

an additional characteristic, namely, thinning of seams is common over anticlines.

In the Kutei Basin, seams are distributed in several areas; Bengalon, Sangatta, Separi-

Santan, Tenggarong, Southwest Samarinda and Balikpapan from north to south

respectively. In terms of the thickness and quality, currently the Sangatta coal

deposit is considered to be the most economic coal in the Kutei Basin.

15

2.3 GEOLOGY OF THE SANGATTA COALFIELD

Geology of the Sangatta Coalfield has been reported by several writers, e.g. Gunawan

(1979), Putra (1978) and Muggeridge (1987). In some oil exploration reports, the

geology of this area is also briefly mentioned (Sikumbang et al. 1981; Vallet, 1983;

Umar et al 1987). However, the most comprehensive coal geological report was

written by Muggeridge (1987). The following sections are mainly based on that

report.

2.3.1 Structural Geology

Geological structures within the coalfield consist mainly of anticlines, synclines,

faults and joints. Folds axes of anticlines and synclines are generally of north-south

direction, whereas faults trend east-west.

Folds

Two major anticlines, the north-south striking Melawan and Pinang Anticlines occur

on the western and eastern sides of the Sangatta Coalfield respectively (Fig. 2.7).

Between the two anticlines is the Lembak Syncline which also strikes north-south.

The Pinang Anticline plunges to the north and south and forms a domed structure

called the 'Pinang Dome' which is the dominant structural element in the Pinang

area. It has been postulated as being of shale of diapiric origin (Gunawan, 1979;

Muggeridge, 1987). Stratal dips in the lower part of the Pulubalang Formation,

which flanks and surrounds the dome, are 15° to 20° on the western, northern and

16

southern sides of the dome and increase to 20° to 40° on the southeast and eastern

sides of the dome. The diapiric structure was believed by Muggeridge (1987) to

have affected the coal rank pattern in the Sangatta area.

The Melawan Anticline, striking from north to south in the western part of the

Sangatta Coalfield, has a long and continuous fold axis regionally. The anticline is

divided into segments based on the name of the area where the anticline occurs. In

the Sangatta Coalfield the Melawan Anticline plunges gently to the north. Stratal

dips in the lower part of the Balikpapan Formation are 15° to 26° on the western

limb and 20° to 35° on the eastern limb of the anticline.

The Lembak Syncline is the only major syncline in the Sangatta Coalfield.

Structurally, the syncline has, to some extent, controlled the distribution of seams.

The syncline is located between the Pinang Dome and the Melawan Anticline and

plunges gently to the north. The limbs of the syncline are commonly gentler than

those of the anticlines. A third order trend surface contour structure map of the top

of the Sangatta seam shows the effects of the syncline on the seam (Fig. 3.11b).

On the eastern limb of the Lembak Syncline, in the northern part of the coalfield,

stratal dips vary from 10° to 20° to the west. The dips become gentler (0 to 15°) in

the southern part of the area where the syncline forms a structurally closed high in

which the coal sequence is exposed entirely across the syncline. First and second

order trend surface structure contour maps of the top of the Sangatta seam indicate a

slight westward tilting of the Lembak Syncline. This may be the effect of doming

of the Pinang Anticline.

17

Faults

Faults can be categorised into major and minor faults. Major faults have caused

significant displacements of seams both geologically and technically. Most of the

minor faults are characterised as growth faults which are more significant in terms of

the depositional environment analysis.

The Villa and northern unnamed fault zones are two major faults which border the

Sangatta coal deposit in the southern and northern parts respectively (Fig. 2.7). The

two normal faults form a structural horst. The Villa Fault, with a fault zone 100 to

500 m wide, has significantly displaced the seams in the northern block, where they

are upthrown by approximately 400 m. The northern normal fault, whose fault zone

is approximately 100 to 200 m wide, has upwardly displaced the seams in the

southern block of the fault by approximately 50 m.

The direction of the minor growth faults varies from north-south to east-west. These

growth faults are aligned in a north-south direction and were probably active during

the peat deposition stage of the Sangatta seam (Muggeridge, 1987). These faults

caused major splitting of the Sangatta seam.

Other growth faults striking east-west, were also probably active during the

deposition of the Sangatta seam. These faults have displaced the seam by some 5 to

20 m and are commonly associated with slickenside fractures in mudstones and

siltstones. The positions of the fractures are parallel or sub-parallel to the bedding

plane.

18

The polished slickenside fractures are most common in blocks E-East, H-South and

B-North and less noticeable in blocks E-West, H-North, D and K.

2.3.2. Stratigraphy and Sedimentology

Three lithostratigraphic units occur in the Sangatta Coalfield; the Pemaluan,

Pulubalang and Balikpapan Formations (Fig. 2.8). The stratigraphic contacts between

adjacent formations are commonly gradational.

Pemaluan Formation

The Pemaluan Formation (Early Miocene) is the lowermost stratigraphic unit in the

Sangatta Coalfield. The formation consists of mudstones, siltstones, sandstones,

marls and limestones. Seams are rarely found in this formation. Thick coralline

limestone lenses equivalent to the Bebulu Formation in the central and southern parts

of the Kutei Basin are also recognised in the Sangatta Coalfield. The limestone

occupies the upper part of the Pemaluan Formation and appears to be the boundary

between this formation and the overlying Pulubalang Formation. In the Sangatta

Coalfield, the Pemaluan Formation has a restricted distribution and only occurs in the

core of the Pinang Dome. The thickness of this unit is approximately 2000 m

(Samuel and Muchsin, 1976; Rose and Hartono, 1978; Sikumbang et al, 1981;

Muggeridge, 1987). The Pemaluan Formation is thought to have been deposited in a

shallow marine environment.

19

Pulubalang Formation

The Pulubalang Formation conformably overlies the Pemaluan Formation. This

formation is characterised by the presence of significant seams. However, the

formation still shows marine influences, especially in the lower part which has

calcareous sandstone layers and several thin coralline limestone lenses. In the upper

part, the formation is characterised by several fluvio-deltaic sedimentary sequences

starting with sandstone bodies at the base and mudstones with coal seam

intercalations at the top. Coarsening-upward sequences are also c o m m o n in this

formation.

In the Sangatta Coalfield, the Pulubalang Formation is distributed mainly in areas

surrounding the Pinang D o m e and along the western margin of the coalfield. Lateral

lithologic facies changes are observed in this formation; on the eastern side of the

Pinang D o m e , the Pulubalang Formation has more marine characteristics than that on

the western side. Gradually, the characteristics of the Pulubalang Formation also

change vertically becoming more like the overlying Balikpapan Formation.

From a sedimentological point of view, in the Sangatta Coalfield, the Pulubalang

Formation may be equivalent to the Loa Kulu Formation in the Samarinda area as

reported by Jones (1981). The significant difference between these formations is the

lack of volcaniclastic sediments in the Sangatta Coalfield. This may imply a

difference in the provenance. If the presence of volcanic glass in the green

sandstone, as reported by Nas and hidratno (1979) and Jones (1981), in the

Samarinda area is considered to be the result of a volcanic eruption, the lack of such

materials in the Sangatta Coalfield suggests a significant difference in the distance

20

from the volcanic centre.

Balikpapan Formation

The Balikpapan Formation is dominated by mudstones, siltstones, and sandstones.

Sikumbang et al. (1981) indicated that the upper part of the Balikpapan Formation

contained limestone beds. However, in the Sangatta Coalfield, the formation is

characterised by several features; absence of calcareous sandstones, more and much

thicker seams, a more fluviatile nature and the absence of coralline limestone lenses.

These characteristics indicate that the Balikpapan Formation is comparable with the

Parangat and Kamboja Formations in the Samarinda area as described by Land and

Jones (1987).

The Balikpapan Formation contains the main coal-bearing strata in the Sangatta

Coalfield. The most economic seams in this formation occur on the western side of

the Pinang Dome. Facies changes occur from west to east over the dome. Coralline

limestone beds found to the east of the Pinang Dome are correlated with the

economic coal-bearing strata in the western area. These may be the limestone beds

in the upper part of the Balikpapan Formation described by Sikumbang et al. (1981).

In the Sangatta Coalfield, Muggeridge (1987) divided the Balikpapan Formation into

three intervals; sandstone, economic coal and high moisture coal intervals. The

sandstone interval is located in the lower 100 to 150 m of the formation and is

dominated by thick sandstone beds especially on the western flank of the Pinang

Dome where the sandstone beds are well developed in southern and northern regions,

whereas in the middle region mudstone, siltstone and coal seams are developed.

21

Sandstones are 5 to 35 m thick and generally fine- to medium-grained sediments

with cross-bedding. Erosive bases with coarse pebbles, including coal, shale and

ironstone intraclasts, are common in these sandstones. In general, the sandstone

interval consists of several genetically-related stratigraphic units starting with

sandstones at the base and grading upwards into siltstone, mudstone and

carbonaceous shale or coal at the top. However some parts of the stratigraphic units

only consist of sandstone bodies which form sandstone sequences up to 40 to 50 m

in thickness.

The economic coal interval, 350 m thick, lies above the sandstone interval. This

interval contains the most economic seams in the Sangatta Coalfield. The main

lithologies are mudstones, siltstones, sandstones and coals. In general, sandstones

with fining-upward features change gradually into siltstones and mudstones which,

together, form a genetically-related stratigraphic unit. Detailed sedimentological

features are discussed in Chapter 3.

In the economic coal interval, 15 seams occur with thickness ranging from 0.3 to

14 m. Seat earths and rootlet beds are commonly associated at the floor of the

seams and shaly coals are common at the base and top of the seams. In terms of

the thickness and quality, the Sangatta seam is the most important seams in this

interval. A more detailed description of the coal geology is given in Chapter 4.

The sequence above the economic coal-bearing strata is more than 500 m thick and

also contains twenty seams. The lithological characteristics of the associated rocks

are also more or less similar to underlying strata. The only distinctive characteristics

are the higher moisture content of the coal compared with underlying interval. The

22

coal is assigned as high moisture coal.

2.3.3 Environment of Deposition

During the deposition of the Pemaluan, Pulubalang and Balikpapan Formations, the

area covered by the Sangatta Coalfield probably experienced a regression. The style

of deposition switched from shallow marine to delta and then to fluviatile

environments.

The Pemaluan Formation was probably deposited within a shallow marine

environment. This is indicated by the associations of mudstones, marls, calcareous

mudstones and calcareous sandstones. Coral reefs are found at the top of the

formation and are indicators of clean, quiet and shallow water. The environment of

deposition changed gradually from open marine to a terrestrial setting. The transition

can be observed through the sedimentary rock association of the overlying Pulubalang

Formation. The lithological characteristics of this formation changes gradually from

marine-influenced in the lower part to fluvial-influenced in the upper part. Deltaic

sedimentation probably took place during the deposition of the middle part of the

Pulubalang Formation which is characterised by coarsening-upward sandstone bodies

associated with bioturbated mudstones. Lateral changes in the depositional

environment may also have occurred during the deposition of the Pulubalang

Formation, particularly from fluviatile in the west to shallow marine in the east.

Most of the strata in the Balikpapan Formation were deposited through the process of

vertical aggradation, progradation and lateral accretion within a set of fluvial

environmental systems. Each system can be separated into several sub-systems such

23

as channel, natural levee, crevasse splay and backswamp. From the lithological

associations, the system can be interpreted as a meandering river system. Washouts

(mainly in the eastern area), splitting and growth faulting of the sedimentary strata

were c o m m o n during deposition. Active differential compaction soon after the

sediments accumulated is also seen in this area.

Lateral changes in depositional settings of the Balikpapan Formation were mainly

from fluviatile in the west to deltaic and shallow marine in the east. Palaeocurrent

measurements indicate that the direction of deposition was from northwest to

southeast. This is consistent with the regional palaeo-environmental data given by

several previously-cited authors.

24

25

CHAPTER THREE

SEDIMENTOLOGY OF CLASTIC INTERSEAM DEPOSITS

3.1 INTRODUCTION

The study of clastic depositional environments has been applied to coal exploration

on both regional and local scales. On a coal basin scale, environmental diagnosis is

commonly used to delineate the coal-bearing clastic sediments. At the coalfield

scale, the knowledge of clastic depositional environments is beneficial for defining

coal seam thickness and quality distributions as well as to determine the mechanical

conditions of the roof and floor strata of the coal deposits (see Home et al, 1978;

Guion, 1987; Ferm and Staub, 1984; Flores, 1983; Peng, 1986). A critical discussion

by McCabe (1984, 1987) suggested that an integrated study including clastic interval

sedimentology and coal seam characterisation should be undertaken to determine the

depositional environment of coal deposits.

The aim of this chapter is to interpret the depositional environments of clastic

intervals adjacent to the Sangatta seam. The study is based on an analysis of

outcrop (locations in Fig. 3.1) and drill hole data including lithologic and geophysical

logs (locations in Fig. 3.2).

3.2 GENERAL DESCRIPTIONS

A sequence comprising limestone lenses and mudstone, with thin coal beds, is

considered to be the base of coal-bearing strata in the Sangatta Coalfield (Fig. 3.3).

26

The sequence is distributed from south to north along the eastern margin of the

coalfield, but is best developed mainly in the northern part of the area. It can be

correlated with the Bebulu Formation in the central Kutei Basin.

Vertically, this limestone and mudstone sequence gradually changes into the fluvio-

deltaic succession of the Pulubalang Formation with seams in the upper part. This

succession is characterised by fining-up channel sandstone bodies in the upper part

and coarsening-up deltaic deposits in the lower part. Some thin fine-grained

calcareous sandstone and limestone beds are associated with the fine-grained

sediments. In areas west of the Sangatta Coalfield, several economic seams such as

the Pamungkas, Tempudan, Jorang, Benu and Melawan seams occur in a sequence

which is correlated with this fluvio-deltaic succession (Fig. 3.4)

In the Sangatta Coalfield, above the fluvio-deltaic sequence lies the Sangatta Coal

Measures which contains the economic coal. The Sangatta seam is the most

important and best dated seam in the coal measures. Below the Sangatta seam, the

coal measures comprise sandstone, siltstone, mudstone and coals with the proportion

of sandstone being approximately 30 percent of the succession. Several seams, with

the Prima, Bintang and B2 seams being the thickest, are associated with these clastic

strata. In a similar stratigraphic position in the Melawan area (west of the Sangatta

Coalfield), the proportion of sandstone is somewhat greater (60%) and seams are

normally thinner (Kaltim Prima Coal, pers. comm., 1992).

Above the Sangatta seam the clastic interval is dominated by fine-grained sediments.

This interval is characterised by the occurrence of thicker seams such as the Middle,

Ml, Pinang, PI, P2, P3, P4, P5, P6, Mandilli and Kedapat seams (Figs 3.5, 3.6).

27

The facies details of the clastic intervals below and above the Sangatta seam are

described in the following sections.

3.3 THICKNESS AND MAJOR LITHOLOGICAL VARIATIONS

The thickness and lithology of clastic intervals below and above the Sangatta seam

vary laterally and vertically quite markedly. The study of the thickness and

lithological variations has contributed to the interpretation of the depositional

environments for the clastic intervals and hence for the seams.

B2-Sangatta interval

In the southern part of the Sangatta Coalfield, where drill holes penetrated the

Sangatta and B2 seams, the isopach map (Fig. 3.8) indicates a thinning of the B2-

Sangatta clastic interval from 40 m in the southwest to 0 m in the northeast (Fig.

3.8b). From the map, it can be implied that the B2 seam appears to be a split at

the bottom of the Sangatta seam. This splitting probably commenced as a result of

differential compaction toward the southwest in the underlying sediments followed by

clastic sediment incursion. The zone where the Sangatta-B2 interval is a minimum

(along and northeast of the zero line) probably represents a thick channel sand belt

below the seams. This channel sand is observed in HT-9, between H-south and H-

north mining blocks and the detail sections are shown in MS-8 of Figure 3.24 (see

section 3.2.1). In the centre of this belt the two seams (the Sangatta and B2 seams)

are absent. This is also indicated by a major northwest-trending washout zone in the

centre of the Sangatta Coalfield. The deposition of channel sands between the B2

and Sangatta seams was confined to the zone where subsidence was greatest, that is,

28

in the southwest area (Fig. 3.9). These sands may also have contributed to the

thicker B2-Sangatta interval in this zone.

Sangatta-Middle interval

The thickness of the clastic interval between the Sangatta and Middle seams varies

remarkably. A low goodness of fit obtained from a trend surface analysis (1st

order= 0.43, 2nd order= 0.62 and 3rd order= 0.73) indicates a low uniformity in the

thickness. The first order trend surface shows an increase in thickness from 15 to

35 m to the northeast (Fig. 3.10b). A strong positive northwest-trending thickness

anomaly in the middle of the area is observed from the residual m a p (Fig. 3.10c).

This zone is also clearly seen as a trench through the structure contour m a p of the

top of the Sangatta seam (Fig. 3.11a) and the 3D-structure diagram of the top of the

Sangatta seam (Fig. 3.1 Id). This could be interpreted as channelling into the top of

the seam, probably during the peat stage.

The negative thickness anomaly for the clastic interval, particularly in the

southwestern part of the coalfield, could be a doming effect of the Sangatta peat bog

during deposition of clastic sediments in the surrounding area (Fig. 3.10a). This

interpretation is consistent with the positive anomaly obtained from the third order

trend surface of structural data (Fig. 3.11c). This zone was probably already higher

than the surrounding area before folding, that is, because of pre-tectonic uplift. A

low sand percentage in this zone (as shown by Figs 3.12a, 3.12c) also indicates that

during Sangatta peat deposition this area was away from the main centre of clastic

sedimentation, especially sand (that is, it was probably above the regional water

level).

29

A narrow zone of thicker clastic sediments in the Sangatta-Middle seam interval,

trending northwesterly as shown by a positive anomaly zone (Figs 3.10a, 3.10c) in

the southern area may be an effect of syndepositional faulting active immediately

after Sangatta peat deposition. This zone was continuously subsiding and filled by

clastic sediments until the time of deposition of the Middle seam.

A comparison of the thickness and sand percentage maps for the Sangatta-Middle

interval shows a relationship between these two parameters (Figs 3.10a, 3.12). This

may be explained by a combination of sedimentation and compaction effects. Sand

deposition will be concentrated in, and tend to fill, low areas probably caused by

growth fault subsidence. Similar situations have been reported by Haszeldine (1989)

in a Late Carboniferous coal deposit in northeast England where higher portions of

sand (found in a faster subsiding zone) are less compactable which, in turn, produces

a relatively thicker clastic interval than in the surrounding areas. Data supporting the

concept of syn-depositional faults and differential compaction structures are

commonly found in many outcrops in the Sangatta study area (see section 3.3.7 and

also Fig. 3.5b).

Vertically, the proportion and thickness of sandstone bodies increase toward the top

of the Sangatta-Middle seam interval. The number of sand bodies also increases

upward. In this interval the main channel sands are concentrated near the top of the

interval, except for the major channel sand in the middle of the area.

30

Sangatta-Pinang interval

The clastic interval between the Sangatta and Pinang seams, including the Sangatta-

Middle seam interval, also varies in thickness and lithology both laterally and

vertically. The thickness increases slightly from 45 to 70 m eastward (Fig. 3.13). A

higher fit obtained from the first order trend surface analysis (R = 0.54) indicates a

higher regularity of the thickness in this interval. However, a strong positive

anomaly in the north and a negative anomaly in the west are evident (Fig. 3.13c)

The percentage of sand increases to the northwest from 10 to 35 percent (Fig. 3.14).

An elongated northwest-trending positive anomaly for the percentage of sand in the

centre of area (Fig. 3.11) probably indicates that channel sand bodies are still

concentrated in this zone as they were for the Sangatta-Middle seam interval. The

negative anomalies on the sand percentage residual map are still observed in the

southwestern, southern and northern parts of the map. One reason for these

anomalies is the scarcity of clastic sedimentation in these areas.

Particularly in the western area, the zone with the negative anomalies on both the

thickness of the clastic interval and the sand percentage residual map could be

interpreted as an elevated area for a period of time while rapid clastic sedimentation

was taking place in the surrounding areas. In this zone deposition of the Sangatta

peat continued until inundation of the peat surface was caused by relatively rapid

compaction in adjacent areas. Considering the compaction ratio of clastic sediments

and peat, the thinnest Sangatta-Pinang interval would be expected in this zone.

In general, the proportion of sand and the number of sand bodies increases upwards

31

to the top of the Sangatta-Pinang clastic interval.

3.4 FACIES DETAILS

Facies descriptions are based mainly on outcrops and drill hole data. Because of

major differences in the mode of sedimentation, coarse and fine-grained facies are

described separately.

3.4.1 Coarse-grained facies

Coarse-grained facies are dominated by fining-upward sandstone and thinly bedded

sandstone. In some places, thick and thin coarsening-upward units are also observed.

Fining-upward sequences

Fining-upward sequences are common in the clastic intervals both below and above

the Sangatta seam. The sequences are commonly composed of associations of pebbly

sandstone at the base gradually fining-up into medium-grained in the middle and

fine-grained or silty sandstone at the top. Lower contacts are mostly sharp or

erosional (Fig. 3.15a), upper contacts are either transitional or sharp. The stacked

sandstone bodies with concave-up bases are indicated on the interpreted cross-

sections (Fig. 3.16). Multistorey fining-upward sandstone units are common within

the interval below the Sangatta seam and in upper part of the Sangatta-Pinang

interval. Lateral accretion structures are also found at the top of some sections (Figs

3.17b, 3.18). Variations in the vertical development of fining-upward sequences

recognised from the shapes of gamma-ray logs are summarised in Figure 3.19. Some

32

of the gamma-ray logs are shown in Appendix 3.1. These fining-upward sandstones

were probably deposited in different types of fluvial channels and different positions

of the same meander channels (Jackson, 1976; Werren et al, 1990). Werren et al

(1990) indicated that fining-upward sequences with blocky-shapes frequently occurred

in the central parts of a point bar complex, whereas bell-shapes are commonly well

developed along the margin of the fluvial channel. In the Wabash River, Jackson

(1976) observed that well-developed, fining-upward sequences (bell-shape) commonly

formed in the downstream part of the meandered belt, whereas in the upstream part,

intermediate and transition sequences (blocky-shapes) were more common.

Pebbly sandstone beds have a thickness varying from centimetres to decimetres.

They are commonly coarse- to medium-grained and normally poorly sorted. These

sandstones are composed of quartz (some polycrystalline and overgrowth quartz),

chert (some radiolarian chert), feldspar, lithic and coal fragments (Table 3.1). Many

of these sandstones contain mud and coal clasts ranging from millimetres up to

20 cm in diameter. The coal clasts are commonly sub-angular, but in places angular

and sub-rounded to rounded clasts are also found (Fig. 3.15a). In some basal

sandstones, coal clasts are oriented along bedding planes. Low angle planar cross-

beds, up to 25 cm thick, are common in these units (Fig. 3.15b). Some of the cross-

beds show truncated and erosional lower contacts (Fig. 3.15c). In places, planar beds

are also recorded (Fig. 3.15d). Occasionally, basal pebbly sandstones are very thin,

as observed in location TD-3b (Fig. 3.18). Siltstone lenses are also found at the

base of some fining-up sequences (for example, MS-3).

Medium-grained sandstones are moderately to poorly sorted. They are composed of

sub-angular to sub-rounded grains of quartz, chert, rock fragments, feldspar and coal

33

clasts (Fig. 3.33). Some are dominated by volcanic rock fragments (Figs 3.33c,

3.33d). Tourmaline, zircon, chalcedony, mica and opaque minerals are also found in

most sandstone samples. Some sandstones contain a calcareous matrix and cement

that has been interpreted as a replacement mineral.

Planar and trough cross-beds are very common in these sandstones with the sets

become thinner upward. In places, fine-grained intercalations are also found between

these sandstone beds (Fig. 3.15e). Some show lateral accretion bedding which may

also be indicated by local angular unconformities between inclined strata in the upper

part of the medium-grained sandstone units and the overlying sub-horizontal fine

grained sediments. Lateral thinning and fining of the sandstones is also observed in

some places (Fig. 3.15f). The base of the medium-grained sandstone is normally

gradational from coarse- to medium-grained sandstone; the upper contact may be

gradual or sharp. These medium-grained sandstone units commonly show progressive

changes into fine-grained sandstone and silty sandstone toward the top of the fining-

upward sequences. However, some geophysical logs indicate that such changes are

not consistently present (see Appendix 3.1).

Cross-beds (5 cm thick and 15° dip) are observed in some medium-grained

sandstones (DH F5304). Water escape structures are also present in this type of

sandstone (MS-3 and MS-6).

In HT-1, the middle part of a fining-upward sequence shows tabular cross-beds

changing vertically into thinly-bedded, medium-grained sandstone. In some places

massive sandstone bodies with poorly defined bedding occupy most of the middle

part of some fining-upward sequences (TD-3c).

34

Below the Sangatta seam, fining-upward sandstone units recognised from several

outcrop sections and from lithological and geophysical well logs (MS-1, MS-2, M S -

3, MS-5, MS-6, C2442, C2579, C2926, C2982, C3031, C3041, C3136, C3486,

C3539, C4041, R2435, F2713, F5304 and F5253) show a thickness varying from 1 to

15 m. Multistorey sandstone bodies are common in this interval and some are

observed in MS-1, MS-2, MS-3 and MS-7. In the E-West area, a channel sandstone

body was recorded in two drillholes (C3486 and C2982) and showed a southeast

orientation.

In the clastic intervals above the Sangatta seam, the thickness of fining-upward

sandstone bodies commonly varies from 2 to 8 m. They are commonly single story

bodies stacked between fine-grained strata. But in drill hole C2331 (Figs 3.5b, 3.6a)

and outcrop EW-1 (Fig. 3.17), in the western part of the study area, two-storey

sandstone bodies are also found. The thickness of the fining-upward sandstone

bodies increases toward the top of the succession. The fining-upward features also

vary from well developed (bell shaped) to intermediate or transitional (blocky)

according to Jackson's (1976) terminology, as indicated by the gamma-ray logs (Fig.

3.19). The multiplicity of sand bodies increases to the north of the study area.

Erosional and scoured surfaces commonly found at the base of fining-upward

sequences may be the result of migrating channels as discussed by Levey (1978).

The presence of lateral accretion structures mainly in the upper parts of the

sequences is the product of progressive lateral shifting of the rivers. M u d and coal

intraclasts in the bottom parts of the fining-upward sequences are lag deposits. The

clasts were probably produced from bank collapse and basal scouring since some

seams are cut or eroded.

35

The preservation of the mud and coal clasts in sandstone bodies requires low energy

levels. In fluvial river systems, this would be determined by factors such as slope,

size and sinuosity of the rivers. In meandering river systems, more specifically, the

level of energy is also controlled by the position within the meander belts, that is,

the concave sides would be of higher energy than that of the convex sides. To

erode consolidated muds and peats, on the other hand, extremely high energy is

required. In the study area, both sedimentological phenomena (that is, mud and coal

clasts in sandstone and eroded mud and coals) are associated with each other.

From the sedimentological characteristics, it is thought that most sandstone bodies in

the study area are unlikely to have been deposited under very high energy regimes.

Therefore, collapses of river banks, due to undercutting, are believed to be the source

of mud and peat clasts which were, in turn, deposited in the convex lower energy

point bars in the meandering rivers.

The presence of sub-rounded coal clasts in most lag deposits may indicate that the

collapse or scouring occurred during the peat stage of coalification. Alternatively,

these clasts could be the product of long distance transportation from older seams.

Petrographic examination of some of the coal clasts, however, shows similar maceral

compositions and a slightly lower vitrinite reflectance (degree of coalification) than

the associated seam. Both refracted and reflected light microscopic examinations

indicate that the majority of coal clasts in sandstone samples may have experienced a

ductile coalification phase before significant compaction of the sandstone (Figs 3.33g,

3.33h). In addition, significant pyrite (especially framboidal pyrite) in many coal

clasts suggests that the clasts may have originated from the upper eroded parts of the

accumulated peat (see Section 4.6). This may support the first interpretation, that is,

36

the sub-rounded coal clasts were transported only short distances as peat mats from a

nearby area.

Truncated surfaces associated with cross-beds at the base of some fining-upward

sequences may indicate fluctuations in the flow regime at the time of deposition

(Haszeldine, 1983). Water escape structures may also suggest that fluctuations of

water depth occurred during deposition (Plint, 1981; Jones and Rust, 1983; Rust and

Jones, 1987). The presence of planar bedding in the basal sandstone of some fining-

upward sequences implies that sedimentation took place under a fairly shallow water

body and probably periodically.

The presence of significant amounts of fine-grained sediment at the top of the fining-

upward sequences indicates that these channel sands were deposited in mixed-load

channel systems. Schumm (1977) pointed out that 5 % to 2 0 % fine-grained sediment

is usually associated with mixed-load stream deposits.

Thinly-bedded sandstones

Thinly-bedded sandstone units are commonly fine-grained with very thin mudstone

intercalations. Small-scale cross-beds are common in this unit (Fig. 3.15g). The

bedding, mostly planar, varies in thickness from centimetres to decimetres (with an

average of 10 cm) thinning-up into well-laminated siltstone (Fig. 3.15h). Syn-

depositional deformation structures such as slump structures and growth-faults are

also recorded in this unit (Figs 3.151, 3.20a).

, a thinly-bedded sandstone unit is underlain by cross-bedded, medium-

37

grained sandstone. In drill holes F5253 and F5304 thin carbonaceous mudstone and

coal beds are intercalated within the thinly-bedded sandstone units (Figs 3.21, 3.22).

Thinly-bedded, silty sandstone is commonly found above fining-upward sequences

and has a thickness varying from decimetres to 16 m. Mostly, the sequences are

composed of intercalations between mudstone and fine-grained sandstone or silty

sandstone with carbonaceous laminae. In places, thinning and fining-upward was

also observed in this type of sequence.

A lateral decrease in grain-size and bedding thickness is typical in this thinly-bedded

sandstone (Figs 3.20b, 3.23b). In ROM-1, HT-7 and HT-2, thinly-bedded fine

grained sandstone units appear to occur as 'multiple wings' on the main sand body.

In CN-1, thinly-bedded fine-grained sandstone shows syn-depositional tilting when

compared with the underlying seam (see section 3.3.7).

The thinly-bedded, fine-grained sandstones which vertically and laterally grade

progressively into well-laminated silty mudstone were probably deposited as overbank

sediments. Slump structures in the lower part of the sequence indicates proximal

levee deposits. The vertical development from the levee to floodplain deposits may

be a result of progressive lateral migration of the main channel toward the cut bank

sides. The presence of fining-upward, thinly-bedded silty sandstone beds overlying

fine-grained strata may indicate abandoned channel deposits, as noted in the

Hawkesbury Sandstone by Rust and Jones (1987).

The presence of thin intercalations of coaly materials in some thinly-bedded silty

sandstones suggests that the overbank areas may have been vegetated. Alternatively,

38

these coaly materials were deposited from suspended organic materials transported

into the overbank area during flooding events.

Coarsening-upward sequences

Coarsening-upward sequences are commonly composed of thin to medium sandstone

beds with fine-grained laminae. Grain-size and bed thickness normally increase

upward as shown in the upper part of MS-5 (Fig. 3.24b). The sandstones commonly

show parallel, ripple, cross and lenticular laminations and locally contain coal

fragments.

Coarsening-upward sequences can be differentiated into thick and thin units. The

thick units are commonly composed of medium- to coarse-grained sandstone with a

thickness varying from 3 to 10 m. The sequences are usually underlain by

bioturbated silty sandstones which gradually change upward into laminated sandstone.

In the middle part of this sequence, cross-beds (normally 10 c m thick and 25° dip)

are observed (drill core F5253; Fig. 3.21).

Pebbly sandstones with sub-rounded coal clasts (up to 3 cm diameter) are found in

the upper part of the coarsening-upward sequences. Coal and mud streaks are very

common in this type of sequence. The sequences are typically overlain by fine

grained sediments with sharp contacts but in places they may be followed by fining-

upward sand bodies.

Thin coarsening-upward sequences are normally fine- to medium-grained. The

thickness varies from 50 cm to 2 m and the basal contact is commonly sharp. The

39

lower parts of some coarsening-upward sequences are bioturbated and contain clay

pellets, coal streaks and dirty silty mudstone with high plant material concentrations

(Fig. 3.20c). Trough cross-beds found in the thin coarsening-upward sequences are

normally 10 cm thick and have a dip of 25°. This type of unit is commonly stacked

within bedded silty mudstone or massive claystone. On the south bank of the Siera

Tenggo River, 50 m northwest of drillhole R840, coarsening along the primary

depositional slope was observed in a coarsening-upward unit containing medium-

grained cross-bedded sandstone (Fig. 3.25b). This has been interpreted as a proximal

crevasse splay deposit.

Coarsening-upward sequences are mainly produced by prograding sedimentation

(Galloway and Hobday, 1983). This commonly occurs in delta, crevasse splay and

alluvial fan environments. Gersib and McCabe (1981) stated that thick sequences

represent deltaic sedimentary associations whereas thin sequences are crevasse splay

deposits. However, Galloway and Hobday (1983) stated that thick sequences

comprising coarsening-upward units can also be found in crevasse splay deposits

produced by 'flood-prone' rivers.

In the study area, because no evidence has been found for the development of bars

by deltaic progradation, both the thick and thin coarsening-upward sequences can be

attributed to crevasse splay deposition. In addition, the absence of deformation

structures, lack of prodelta mud and absence of marine associations in most sections

also suggests that the sequences were not produced in major marine deltaic

environments, but probably only in small-scale deltas that prograded into lakes (Fig.

3.21). The presence of mud clasts, poorly-sorted silty sediments and high

concentrations of plant material at the bottom of some coarsening-upward sequences

40

(Fig. 3.20c) indicates flood deposits with rapid and dirty sedimentation (Galloway

and Hobday, 1983).

3.4.2 Fine-grained facies

Fine-grained facies are dominated by laminated and massive mudstone and siltstone.

X R D analysis indicates that the fine-grained lithologies contain quartz, clay minerals,

feldspar and mica (Fig. 3.26; Table 3.1). Kaolinite is the most c o m m o n clay mineral

in the sediment, although montmorillonite, illite and chlorite are also present, mostly

as mixed-layer clays. Coal beds are mostly associated within the fine-grained facies.

Laminated fine-grained sediment

Laminated, fine-grained sediments are composed of intercalated mudstone, siltstone,

fine-grained sandstone and plant fragments. Laminated mudstone consisting of

alternating mudstone and carbonaceous/plant fragments is also c o m m o n in this

sequence. Both types normally show parallel and lenticular laminations. Ripple

laminations in siltstone are also found in places. Some indefinite wispy laminae are

produced by oriented leaf or plant remains. In places, disturbed laminae, probably

caused by bioturbation, also occur. Ironstone nodules are found along the bedding

planes in the laminated mudstone.

Coal lenses, coal fragments and logs are common in the lower parts of some

laminated mudstone indicating that parts of this association were deposited within

abandoned channels in which bank coEapse or periodic flooding may have supplied

the peat fragments and logs.

41

Vertical changes in carbon content are observed in the laminated mudstone units

which may indicate changes in the hydrologic conditions during deposition. Vertical

changes in the abundance of silty sand probably resulted from changes in intensity of

water flow. The preservation of large plant remains suggests that at some period the

water in this area was quite deep. Because most of the logs have been completely

coalified, rapid burial of the logs by fine-grained clastic sediments must have

occurred to protect the logs from decomposition. Alternatively, the logs may have

been deposited within an anoxic lake with slower sedimentation.

In drill core F5304, typical associations of fine-grained sedimentary units were

observed. At this location, laminated mudstone units are commonly overlain by

calcareous nodule-bearing massive mudstone indicating soil formation.

In general, the abundance of intercalated carbonaceous materials associated with fine

grained sediments increases toward the top of the sequence.

Laminated, silty mudstone units interpreted as the base of abandoned channel

deposits, are found in the C-North and Hatari Mines. Cross-laminations in laminated

silty sandstone above the Pinang seam in E-West Mine were used to determine

palaeocurrent directions at this location.

The laminated, fine-grained sediments have been thought to be deposited in a

floodplain setting (probably with some shallow lakes). The water depth may have

controlled the occurrence of lake deposits and soil development. The changes in

grain size and the thickness of laminae may reflect the distance from the centre of

the fluvial system, in this case the main river. The presence of several layers of

42

clayey ironstone nodules can be interpreted as cyclic soil development that occurred

in the floodplain area. The organic-rich intercalations may indicate that the

floodplain was occasionally vegetated or swampy.

Massive fine-grained sequences

Massive fine-grained sequences are predominantly composed of mudstone, with rare

silty intercalations. The thickness of these sequences varies from 1 m to several

metres. The carbonaceous content, appears to control the colour of the mudstone

which varies from dark to light grey in colour. This m a y indicate waterlogged

conditions or soil development during the formation of the mudstone. Leaf fossils

found in this lithology (Fig. 3.20d) sometimes imparts a faint lamination to the

facies.

In location HT-3, light grey massive mudstone underlies the Sangatta seam. Coal

lenses are present in the upper part of the mudstone, increasing in intensity and

thickness upward (Fig. 3.20e). Coalified logs also occur in the mudstone (Fig.

3.20f). Massive mudstone is also found below the Sangatta seam in E-West Mine

where the massive mudstone changes upward gradually to laminated carbonaceous

shale. A similar feature was also noted in some intervals in the drill core F5304.

The massive light grey mudstone has little carbonaceous material and this probably

indicates a soil development process on the floodplain. The laminated carbonaceous

shale indicates that the soil was slightly vegetated at the top.

In the eastern part of the coalfield, however, the deposition and preservation of logs

associated with the mudstone (in locality HT-2) suggests that the water was quite

43

deep on the floodplain before the accumulation of the Sangatta peat. In this area, a

massive mudstone unit may have been drowned due to a greater subsidence.

Coal beds are common at the top of some massive mudstone units. Ironstone

nodules are also sometimes found in other mudstone units. Bioturbation and burrow

like structures in mudstone, interpreted as root moulds, were observed in some parts

of the massive units.

In the clastic intervals above the Sangatta seam, carbonaceous material is commonly

disseminated throughout the massive mudstone. Some units gradually change to

laminated mudstone vertically.

The considerable thickness of the fine-grained units reflects prolonged aggradation in

overbank areas. The sediments may have been supplied by a 'flood prone' river, but

the massive nature implies a stagnant sedimentary setting (probably a lake) or soil

processes. The presence of kaolinite as the dominant clay mineral in the fine

grained sediments indicates a mature clay mineral suite that perhaps resulted from

reworking of within-basin sediments (Spears, 1987) or leaching during soil

development (Wanless et al, 1969) if the latter interpretation is correct.

Coal beds

Below the Sangatta seam a number of coal beds are associated with the fine-grained

facies with Prima, Bintang, Bl and B2 being the major seams. The seams vary from

decimetres to 10 m in thickness. In general, the seams are predominantly bright

lithotypes (vitrain).

44

The Prima seam is distributed from southwest to northeast and its thickness varies

from 1 to 10 m with the thickest sections in the western, eastern and northern areas.

The seam splits towards the east with a clastic parting up to 0.30 m thick. The

lower half of the seam has a high sulphur content and the seam is commonly

underlain by high sulphur content mudstone. This suggest that the peat

accumulation commenced in a wet swamp where the influence of brackish water was

marked.

The distribution of the Bintang seam shows a north-south trend with the thickness

varying from decimetres to 3 m. The thickest part of the seam is found in the

middle of the outcrop pattern. The lower half of this seam has a low sulphur

content suggesting the absence of marine influence at the early stage of peat

deposition.

The change of sulphur contents in the lower part of the Prima to Bintang seams (that

is, higher in the Prima seam) suggests that the peat swamps, during early stages of

accumulation of both seams, changed from marine influenced to fresh water

environments. This is probably the result of a regression process corresponding to

progradational clastic sedimentation in an easterly direction.

The B2 seam (split of the Sangatta seam) is distributed mostly in the southwestern

part of the Sangatta Coalfield. This seam thins in a southwest direction (Fig. 3.27)

where the incursion of clastic sediment is greater (indicated by channel sandstone and

a thicker B2-Sangatta clastic interval). This is also indicated by an increased ash

yield in the B2 seam toward the southwest (Fig. 3.28). The slight increase in

sulphur content may also suggest an increase in water depth in this direction. The

45

sulphur content is usually highest at the bottom of the seam. The B2 seam has high

vitrinite (87.9%) and telovitrinite (55.5%) contents as observed in coal sample from

EW-6.

Above the Sangatta seam, a number of coal seams are associated mainly with fine

grained sediments. The major seams are the Middle, Ml, Pinang, P1-P6 and

Kedapat seams. The Middle and Pinang seams are considered to be closely related

to the Sangatta seam and are described here.

The Middle seam is 1 to 7 m thick and tends to be better developed in northern part

of the coalfield. In the southern region this seam represents an upper split of the

Sangatta seam. Merging of the two seams formed the thick Sangatta seam in the E-

West area where the two combined coals are named the Sangatta seam. However,

detailed observations of outcrop, drill core and geophysical logs shows that the two

seams can be differentiated if care is taken (see Chapter 4).

The Middle seam thickens to the northeast where the Sangatta-Middle clastic interval

also thickens. In the middle of the coalfield, however, the coal thickness decreases,

probably as a result of washouts and erosion. The presence of a channel is also

indicated by the elongated high sand percentage zone from northwest to southeast

shown on the residual map of the Sangatta-Pinang clastic interval. The zone with

the highest ash content, located in the middle of the coalfield, may be another

influence of this channel.

In general, the sulphur content in the Middle seam increases eastwards from 0.1 to

3%. In the middle of the coalfield the sulphur content increases toward the

46

palaeochannel. This may have resulted from the high inorganic content in the coal

which enabled sulphur to be deposited. Alternatively, the high sulphur may indicate

that the channel was probably influenced by salt water perhaps a tidal channel.

The Pinang seam is 1 to 8 m thick and is thickest in the northwestern part of the

coalfield. In this area the percentage of sand in the Sangatta-Pinang clastic interval

is also highest. In comparison with the Sangatta seam, this feature suggests that the

centre of peat deposition shifted toward the northwest during the Middle seam and

Pinang seam times and this could indicate a transgression process.

3.4.3 Lateral accretion

Lateral accretion structures were found in four localities. The architecture of lateral

accretion deposits varies from location to location. For example, a channel sandstone

body, with lateral accretion deposits, near the middle of the channel (Fig. 3.23b) may

be planar bedded in the lower part of the sequence. This may indicate higher energy

in the centre of the channel. Recognition of the lateral accretion structures was

mainly based on outcrop observations where gradual facies changes from the channel

sand into the levee and floodplain deposits were clearly seen.

In some outcrops, the upper parts of fining-upward sequences, which have moderate

angle stratification, are overlain by sub-horizontal silty mudstone. This relationship

has also been considered to result from a lateral accretion process.

In location TD-3b, a variation in the angle of the lateral accretion surface, from west

to east, was observed (Fig. 3.18b). Toward the eastern edge of the outcrop, bedding

47

is sub-horizontal and the proportion of fine-grained sediment increases. This

indicates a gradual change in the stream energy, that is, a progressive decrease

eastward followed by abandonment at the eastern edge (Puigdefabregas, 1973).

Approximately 50 m west of the western edge of this outcrop the sandstone is

coarser grained and the fine-grained deposits depleted. Lateral accretion surfaces

containing siltstone and mudstone intercalations are developed only in the upper part

of the channel sand body (Fig. 3.18c) and are probably produced by a low- to

moderate-energy mixed-load meandering river (Thomas et al, 1987).

Some well-developed lateral accretion structures in the upper parts of fining-upward

sequences show an upward increase in the proportion of fine-grained sedimentary

intercalations. Thinning and fining of sandstone beds in an up-dip direction are

clearly recognised in these situations (Figs 3.17b; 3.18a). A similar feature has been

documented by Puigdefabregas and Vliet (1978) from a meandering stream deposit in

Spain. This was probably caused by a decrease in both energy and coarse-grained

sediment supply away from the thalweg of the channel. Particularly at location EW-

1 (Fig. 3.17b), the decrease probably occurred quite dramatically in the southern part

of the channel bringing abandonment of this channel due to avulsion in an upstream

part of the channel.

Although lateral accretion structures may be found in various types of depositional

environments, the most common are those associated with point-bar deposition

(Allen, 1965; Thomas et al, 1987; Collinson, 1978). Not all meandering rivers

produce lateral accretion structures (Allen, 1970; Rust, 1984; Thomas et al, 1987).

The development of lateral accretion structures in a meandering river depends mainly

on the proportion of fine-grained sediment supply and the energy level. Lateral

48

accretion structures are not produced by major channels with high energy and high

rates of sand supply (Rust, 1984). Rust (1984) suggested that channel sand bodies

showing lateral accretion are more commonly deposited in tributary channels. They

are most likely to occur when periodic decreases in energy within the river cause

deposition of fine material from suspension.

From the angle of the lateral accretion surfaces (typically more than 15°) it is

suggested that most rivers in the study area were not large. Miall (1981) pointed out

the angle of accretion surface ranged from 1° for very large meandering rivers to 25°

for small rivers. The depth and width of the channels can be defined approximately

by the thickness of the lateral accretion units measured perpendicular to the lower

bounding surface (as suggested by Leeder, 1973). Such measurements indicate

moderate depths and widths for the channels in the Sangatta area. The channels

were 3 to 15 m deep with a typical depth of 5 m; widths vary from 20 to 100 meter

but with typical widths of 50 m.

3.4.4 Facies relationships

Spatial relationships of sedimentary facies are influenced by the style of

sedimentation. Galloway and Hobday (1983) reviewed three types of sedimentation

styles; vertical aggradation, lateral accretion and progradation. Recognition of the

spatial relationships at a field scale was guided by this concept. The concept of

sedimentary facies relationship which states that vertical successions of sedimentary

facies reflect the horizontal relationship of the facies (Reading, 1986, p. 5) was also

applied in the field observations.

49

Spatial facies changes were observed in outcrops and inferred through drill hole

correlations. In outcrops, fining-upward sandstone units commonly occur as stacked

single sandstone bodies and amalgamated multistorey sandstone bodies within fine

grained associations. Towards the floodplain, in many channel sandstone bodies, the

grain size and bedding thickness usually decreases and, in turn, the coarse units

interfinger with fine-grained units (for example, Fig. 3.15f). In the transitional zones,

the development of thinly-bedded sandstone forming levee deposits is quite common.

Lateral facies changes from levee deposits into seams and floodplain facies are

common. In places, in the upper parts of sandstone bodies, the grain size and bed

thickness decrease on both sides of the channel forming 'wing sand' bodies. In this

situation, lateral accretion is not present. Sharp contacts between channel sand

bodies or abandoned channel fine-grained sediment and adjacent strata, resulting from

eroded channel margins, were also observed. Occasionally, complex facies

relationships were also encountered.

Vertically, fining-upward sandstone sequences are usually capped by thinly-bedded

levee deposits. Elsewhere, mudstone or silty mudstone are also found to directly

overlie fining-upward sequences as a result of channel abandonment.

Drill hole correlation was based on lithological and geophysical logs and forms the

basis for interpreting long-spaced facies relationships. Some of the logs are given in

Appendices 3.2 and 3.3. Well-distributed seams are mainly used as the reference

strata. Differences in the sedimentation rate between coarse and fine-grained

sediments was considered when connecting lithologies. The different compatibilities

of sand, fine-grained sediment and coal were also taken into account.

50

The results indicate facies and thickness changes in sandstone bodies stacked in fine

grained strata (Figs 3.5, 3.6). From geophysical logs lateral changes in the structural

development of fining-upward sandstone bodies is also seen, that is, from well-

developed (bell-shaped) to transtional (cylindrical) sequences.

3.4.5 Palaeocurrents

Data used to assess palaeocurrent directions and the hydrodynamic characteristics in

the study area were collected from ten locations. Most measurements are from

cross-beds mainly in channel sandstones. A few data were collected from cross-

laminations in silty sandstones (location EW-3) and log orientations in fine-grained

sediments (HT-3). The directions of lateral accretion surfaces were also considered.

The azimuth, dip and thickness of sets of cross-beds were measured.

Although the regional dip of the strata is generally low (normally less than 20°), a

computer program developed in Fortran-L77 codes by Dr B. G. Jones (University of

Wollongong, N S W , Australia) based on a CDC3600 computer program (Jones, 1970)

was used to correct the field measurements for tectonic tilt. This program produced

the corrected initial orientation of the cross-bed positions and statistically analyses the

data. The results of the computations are attached as Appendix 3.4.

Rose diagrams for each locality generally show unimodal distributions (Fig. 3.30) but

each locality indicates a different palaeocurrent direction. In terms of the general

orientation however, the palaeocurrent data indicates a grand mean direction of 096°

(Fig. 3.31).

51

Palaeocurrent directions in channel sandstones may be used to indicate the palaeoflow

of the river. In one sandstone horizon, different flow directions between locations

suggest sinuosity of the river.

Palaeocurrent directions determined from cross-laminae can be used to locate the

relative position and direction of flow of the main stream. Data from EW-3 show

that the position of the stream was to the north of the location and it was flowing

southeastward.

In mudstone, orientations of logs parallel to the flow directions of the adjacent river

may indicate quite deep flowing water during the deposition of the logs.

The flow directions shown by the palaeocurrent analyses (to the southeast) are

concordant with the decrease in sand percentage to the southeast in the clastic

interval above the Sangatta seam. This probably indicates that the source of the sand

was to the northwest with the sand being transported to the southeast. This is

consistent with the sedimentation pattern in surrounding areas, as reported by

Pattinama and Djunaedi (1977) in the Sangatta oilfield and Biantoro (1988) in the

North Pinang area. Moreover, the local sedimentation patterns are compatible with

the regional pattern of the Kutei Basin postulated by Samuel and Muchsin (1976)

and Rose and Hartono (1978).

3.4.6 Syn-depositional Structures

Syn-depositional geological structures have been found to be associated with a

number of coal deposits (Doveton, 1970; Mallett and Dunbavan, 1984; Weisenfluh

52

and Ferm, 1984; Flood and Brady, 1985; Titheridge, 1988; Haszeldine, 1989; Staub

et al, 1991). In the current study area, various types of geological structures formed

by syn-depositional deformation include large-scale inclined strata, growth faults and

seam splitting.

Large-scale inclined strata were observed in the upper part of a channel sandstone

body overlying above the Middle seam at locality CN-1 (C-North Pit). The strata

are inclined toward the area where the coal is thickest (Figs 3.23a, 3.32b).

Interpreting the original form of the clastic sediment and peat facies relationships

needs correction for compaction factors because compaction is a major syn- and post-

depositional process occurring in both the clastic sediments and peat Compaction

ratios from peat to bituminous coal and from sand to sandstone were given as 10:1

and 1:1, respectively, by Ryer and Langer (1980). In the case of the field

observations at CN-1, however, using a 5:1 peat to coal compaction ratio is probably

more realistic (Fig. 3.32a), because with this ratio the peat surface would have been

located at the same level as the top of the adjacent channel sediments. This is in

agreement with -5:1 compaction ratio suggested by Moore and Hilbert (1992) for

other low rank coals in Kalimantan, Indonesia.

Considerable changes in thickness of the peat on a very local scale would give

greatest 'self-generated' compaction in the thickest zone (Titheridge, 1988). As a

result, the original planar-bedded sandstone has been inclined towards the more

compacted part of the underlying peat as postulated in Figure 3.32b. Therefore the

large-scale inclined strata are thought to be a differential compaction product.

53

Some growth faults were observed in the study area (Figs 3.20b, 3.20g). The

recognition of the faults was based on several diagnostic criteria as reported by Elliot

and Ladipo (1981) for sequences in South Wales where the fault planes do not

continue into the overlying strata and, in outcrop, the fault planes are normally

smooth without accompanying fractures, indicating a pre-diagenetic formation before

lithification. In the Hatari Pit, an oblique growth fault (250730°W) moved the

Sangatta seam down a maximum of 10 m, whereas the upper Middle seam was not

affected by the fault (Fig. 3.34). The downthrown part of the fault was covered with

a greater thickness of clastic sediment as a result of channel sand deposition (location

HT-7).

Major growth faults are interpreted through the correlation of drill hole data (Kaltim

Prima Coal Internal Report, 1988). Two major north-trending normal faults have

been reported to be contemporaneous with the Sangatta-Middle seams in the southern

area of the Sangatta Coalfield. The faults caused major splitting, producing the

Sangatta-Middle split system (for example, Fig. 3.5b). The patterns and magnitudes

of the growth faults were probably controlled by the intensity of differential

compaction in the Sangatta peat and the underlying strata. The scale and intensity of

facies changes are believed to be a major factor causing such differential compaction.

On an outcrop scale, differential compaction effects are reflected by seam splitting

(Fig. 3.20h). The differential compaction probably resulted from changes in the

physical characteristics of the underlying strata, that is, seams split where underlying

sediment changes from sandstone to mudstone (more compactable).

54

3.5. DISCUSSION AND SUMMARY

To interpret the depositional environments of the clastic interseam strata several

sedimentological parameters have been analysed. Thickness and major lithological

variations within the intervals indicate major trends in sedimentation patterns, that is,

from proximal in the west to distal in the east. This is consistent with the grand

mean palaeocurrent direction (096°) and data from the North Pinang area. A similar

sedimentation direction was reported for sandstone in the Sangatta oilfield (southwest

of the current study area).

The sedimentological associations found in the clastic interseam strata show that they

were mainly deposited within a fluvial system. The low proportions of sand in most

intervals (0-35%) indicate a mixed-load fluvial system. The presence of fining-

upward sequences with lateral accretion deposits containing significant amounts of

fine-grained sediment suggest that the channels were mostly meandering. However,

most of the sandstone units found in the upper clastic intervals are relatively small

and may not have been deposited within major channels but rather in low- to

moderate-energy- tributary or anastomosing channels.

Amalgamated sandstone bodies recorded at MS-8 and the major east-trending

washout zone in the Sangatta seam are thought to represent major channels in this

area. The behaviour of these main channels probably controlled the sedimentary

characteristics for this fluvial system. The thick overbank deposits found associated

with the Sangatta seam may have been related to the same drainage system that

discharged from this channel as the main channel was probably stacked in the same

position for a period of time. The fine-grained sediments were probably deposited in

55

floodplain basins ( or shallow lakes). The presence of ironstone layers and seam

intercalations indicates soil development in the overbank areas which were commonly

swampy and vegetated. From the sedimentological data, in the eastern part of the

Sangatta Coalfield the Sangatta peat probably developed on a deeper water platform

compared to the western part.

Seams are associated with the fine-grained floodplain sediments of the fluvial system.

The thickness and quality characteristics of the seams, particularly the B2, Sangatta

and Middle seams, could have been influenced, to some extent, by the behaviour of

the main channel system. Syn-depositional deformation also influenced the thickness

and quality distribution of the Sangatta seam. This was a major factor and caused

splitting and thinning, or thickening, of the seams depending on the locality.

The thickness of clastic interseam strata was controlled by the percentage of

sandstone which, in turn, reflected local subsidence caused by differential compaction

and growth faulting. Thus palaeomorphology is one of the major factors that

controlled the thickness and extent of the clastic strata.

The sedimentological characteristics changed from the lower to upper clastic

intervals, that is, from high energy bed- and mixed-load channel to low- to moderate-

energy mixed-load channel deposits. This may reflect a change in tectonic and

geomorphic styles or climate within the source and deposition zones. The lower

intervals were probably deposited during an active uplift in the catchment area with a

higher depositional gradient, whereas the upper intervals were deposited in a more

mature stage of erosion. Alternatively, this could be the result of a major change in

the drainage pattern of the fluvial system.

56

57

CHAPTER FOUR

COAL SEAM GEOMETRY

4.1 INTRODUCTION

The Sangatta seam is one of the most widely distributed seams in the Sangatta Coal

Measures. It forms the main part of the Sangatta-Middle seam split where the

Sangatta seam in the western area splits eastward into the Sangatta (lower) and

Middle (upper) seams.

The Sangatta seam extends over the southern and northern parts of the Sangatta

Coalfield and, to some extend, the eastern part of the Melawan Coalfield. It is

exposed along the eastern and southwestern flanks of the Lembak Syncline where it

forms a J-shaped outcrop (Fig. 2.7). The J-shape is controlled by the Lembak

Syncline and a facies change since, to the northwest, the seam is not well developed

due to the domination by clastic facies.

An understanding of the geometry of the Sangatta seam involves identification of

roof and floor strata, seam thickness variation, structure and morphology of the seam,

vertical development of the seam, dirt band distribution and seam quality profiles.

This study was facilitated by numerous geophysical logs, lithologic logs, ply-sample

quality data and outcrop observations. The aims are to understand the geometry of

the Sangatta seam in relation to the environment of deposition and, hence, provide a

useful model for geostatistical reserve estimations.

58

4.2 ADVANTAGE OF GEOPHYSICAL WELL-LOGS

Coal has several unique physical properties. For example, coal usually has low

natural radioactivity, low density and high resistance to electrical current. These

properties generally contrast with those of most other rocks in the coal-bearing

sequence. In coal exploration programs, geophysical well-logs are used effectively to

identify seams and to define their boundaries with interseam clastic deposits.

Geophysical well-logs have proved to be a useful tool in many subsurface studies of

coal and coal-bearing strata (for example, Renwick, 1981; Groves and Bowen, 1982;

Hoffman et al, 1982; W o o d et al, 1983; Hutton, 1990). These techniques provide

rapid, economical and detailed information on the lithological characteristics,

thickness and depth of strata (including seams) penetrated by a drill hole. For the

Sangatta Coalfield, after calibrating geophysical well-logs with drill core and cutting

logs, the geophysical logs were extremely useful for identifying vertical and lateral

development of seams and interseam clastic sedimentary sequences (for example, Figs

4.1a, 4.1b).

In the study of the Sangatta seam, gamma-ray and density logs were used to identify

the vertical and lateral development of clean coal benches and dirt bands included

within the seam. In vertical sections, the geophysical logs confirmed the position,

thickness and clay content of dirt bands and clean coal plies. Bed resolution density

(BRD) or coal seam thickness logs were used to accurately determine the depth and

thickness of coal plies and partings.

For correlation purposes, the combination of gamma-ray and density logs

59

(supplemented with calliper logs) define the character of the strata surrounding the

seam and provide a signature for the log responses to the seam (Hoffman et al,

1982). Unlike clastic interseam correlations, which are based more on gamma-ray

logs, the correlation of seams is commonly based on long spaced density (LSD) logs.

In using geophysical and lithological logs for correlating the Sangatta seam, the

concepts of sedimentary facies, sedimentation rates and compactability have been

considered. As a result, the variation in gross and clean coal thickness has been

delineated. In addition, lateral variation in dirt band thickness has also been

identified.

Geophysical logs, particularly long spaced density logs, were used to check ash

yields obtained from chemical analysis. After calibrating the two sets of results,

geophysical logs were used to estimate specific gravity and ash yield of the coal

where cores were not available. The relationship between specific gravity and dried

ash yield for the Sangatta seam is given in Fig. 4.2. The ash yield values indicated

by long spaced density logs have also been used as an estimator for qualitative

organic content in dirt bands and to interpret organic-inorganic facies changes.

4.3 CONTROL OF THE THICKNESS VARIABILITY

Seam thickness commonly includes all the coal plies and silty partings lying between

the roof and floor. It is categorised into gross thickness (including partings) and net

thickness (clean coal).

The Sangatta seam has its greatest gross thickness in the western and northern parts

60

of the Sangatta Coalfield. In some parts of the eastern area the seam is also quite

thick due to the intercalation of clastic partings (Fig. 4.5 ). In the central-southern

part of the coalfield the seam appears to be relatively thin.

In the Sangatta seam, clean coal is thickest in the western and central areas of the

coalfield. Here, the seam consists of two clean coal benches, the lower and upper

benches (Fig. 4.4). The lower bench is the thickest and most continuous bench

(approx. 8 to 10 m thick), becoming thinner and rapidly splitting to the west and

north where more dirt partings developed. The thickness of the lower bench also

decreases slightly toward the central area. The upper bench shows a rapid reduction

in thickness to the west where it grades laterally into carbonaceous clastic strata. In

the central and eastern areas the upper bench becomes split from the Sangatta seam

and is named the Middle seam. The Sangatta-Middle interseam strata range in

thickness from decimetres to 40 m (Chapter 3).

The thickness of clean coal should indicate conditions at the time of coal formation,

because it is manifested as the level of organic development in the seam. During its

formation, clean coal is not reached or affected by significant clastic sedimentation.

The distribution of the thickness of clean coal in the Sangatta seam is probably a

function of the lateral and vertical position relative to the closest active zone of

clastic sedimentation, as well as the water level in the peat swamp. The western,

central and northern parts of the coalfield, where the clean coal is thickest, were

probably relatively far from any active river channels.

In seam model 1 (Fig. 4.3), reconstructed on the basis of lithological and geophysical

logs, the thickest part of the seam has been attributed to a low-lying peat swamp on

61

a floodplain. Overbank sediments, consisting of silty sandstone and mudstone, were

deposited contemporaneously with the peat swamp, and the facies change from

overbank sediments to the lower bench peat swamp occurred between drill holes

F2444 and C3002 (Fig. 4.3a). Thus, the lower coal bench in C3002 and C3007

would be expected to have a high inorganic content since clastic deposition was

occurring less than 200 m from the peat swamp. However, this is not the case as

the lower coal bench is quite clean with less than 2% ash yield (data from ply coal

samples). To explain this condition, the position of the water table in the peat

swamp must have been higher than the regional flooding level and, therefore, it was

not reached by clastic sediment. Coal seam model 2 (Fig. 4.4) may be more

suitable. In this model, the lower bench clean coal initially accumulated in a

floodplain swamp setting above an overbank sequence. As the rate of peat

accumulation increased, the peat surface probably rose forming a tophogenous peat

which, in turn, was not reached by clastic detritus. Elevated inorganic content was

found only in the lowermost part of the peat and is recorded as high ash coal at the

bottom of the seam. This suggests that overbank sediments only influenced the early

stage of the peat accumulation process.

At the time of deposition of the upper part of the lower bench, the central area

began to subside more rapidly, resulting in termination of peat accumulation in this

area, whereas in the western area peat deposition was still maintained. This caused a

thinning of the lower bench towards the central area. Several possible causes would

account for this difference in rate of subsidence.

1. Differential compaction of the peat itself. The initial thickness of peat

accumulating in the central area would undergo greater compaction than

in the surrounding areas.

62

2. Differential compaction of underlying strata. Peat in the western and

eastern areas may be underlain by parts of the channel sandstone facies

as recorded in drill holes C3486, F5304 and C2982 (in west) and in

Hatari Pit (east).

3. Growth faults may have been active at the time of deposition of the

upper part of the lower coal bench.

As the central area subsided to produce a topographic low it was filled with clastic

sediments resulting in thick clastic interseam strata. In some places, the top of the

coal bench was eroded by fluvial channels, as recorded in the eastern part of the

central area (Fig. 4.4).

When the subsidence rate decreased and the central area was re-stabilised, the Middle

seam started to accumulate from the west (as the upper bench of the Sangatta seam)

to the east (as the separate Middle seam; Fig. 4.4). Because more peat was present

in the western area at this stage, differential compaction of underlying strata resulted

in the upper bench of the Sangatta seam being deposited in a relatively low

topographic position. This is probably the reason for the rapid reduction in the

upper bench thickness in the southwestern area where clastic sedimentation was more

active.

Active clastic sedimentation along the western margin of the Sangatta Coalfield also

disturbed the development of the Sangatta peat, therefore, the clean coal thickness

decreases in that direction. In addition, the water table was probably too low to

preserve the peat.

63

In the eastern part of the coalfield the clean coal is split by many clastic bands

indicating a repetition of clastic incursions (probably overbank sediments) into the

swamp during peat accumulation (Fig. 4.5). Each bench of the split coal decreases

laterally in thickness to the east and, in turn, grades laterally into carbonaceous shale

at the eastern edge of the Sangatta seam (Figs 4.5, 4.6a, 4.6b). Fluvial activities are

indicated by the presence of some channel sand bodies correlated with and occurring

above the seam.

4.4 STRUCTURES IN THE SANGATTA SEAM

On a regional scale the Sangatta seam shows a synform, and this is part of the

Lembak Syncline. Elevation data from the top of the seam are well fitted to a

structure contour map obtained from third order trend surface analysis (Fig. 4.7).

However, local undulations shown by the residual map suggest that the top surface

of the Sangatta seam is not very regular. Several possible causes for this irregularity

are:

(i) local faults, including growth faults (Staub et al, 1991);

(ii) initial topography of the peat-dome or low lying peat;

(iii) washout-erosion of the top of the seam;

(iv) diapirs; and

(v) parasitic folds.

Plotting the structural data from the base of the seam, however, shows a relatively

smooth surface. This suggests that parasitic folds and diapiric structures are not the

cause of the undulating upper surface. Therefore a combination of the first three

possibilities is likely to have caused the undulations.

64

The local undulations probably formed before compression gave rise to the Lembak

Syncline. Graphic transformation of the top surface of the Sangatta seam back to an

original horizontal position, with reference to the third order trend surface, indicates

that in the western and eastern areas the top of the seam is higher in position than

for the central region (10 m difference). This suggests that the central region was

already relatively low before the formation of the Lembak Syncline, as also indicated

by the presence of negative residuals on the trend surface. This is consistent with

the previous interpretation (section 4.3) that the central region subsided more rapidly

and parts of the seam were eroded.

The interpretation of local faults (probably growth faults) is supported by the

observation of fourteen small scale faults which only influenced the Sangatta seam

(Kaltim Prima Coal Internal Report, 1988). The throws on the faults were reported

to be from 5 to 40 m. The extremely low zone in the eastern-central area could

have been affected by channelling (washout). However, the thickness of the clastic

interval between the Sangatta and Middle seams in the central area is more than 40

m, indicating that not only has the subsidence separated the two seams but also it

allowed the accumulation of a widespread clastic wedge (less compactable; Fig. 4.8).

4.5 FLOOR AND ROOF STRATA AND PARTINGS

The Sangatta seam is normally underlain by shale or claystone (some show seat

earths). These fine-grained sediments can be laminated or massive. The colour

varies from grey to dark brown as the organic content in the claystone increases.

Slickenside surfaces are common in some claystones. XRD-analysis of the clay

samples reveals that quartz and kaolinite are dominant components of the claystone.

65

Contacts between the underlying sediments and the seam are commonly abrupt, but

gradual contacts from coaly shale to coal are also observed. The thickness of the

fine-grained floor strata ranges from very thick to very thin. In some places, the

Sangatta seam directly overlies the upper part of a fining-upward sandy sequence

(probably a channel or crevasse splay sand).

Roof strata above the Sangatta seam vary from shale to claystone, siltstone or

sandstone. Contacts between the seam and the overlying shale are normally gradual,

characterised by coaly shale at the top of the seam. The thickness of the fine

grained sediment ranges from very thick to very thin. In some places, crevasse

splay/channel fining- and coarsening-upward siltstone or fine-grained sandstone beds

overlie the seam.

Channel sand bodies (Fig. 4.6c) and abandoned channel fine-grained sediments (Fig.

4.5b) are found at the top of the Sangatta seam. An unusual very high porosity in

sandstone overlying the seam could be the result of dissolution of the cement by acid

solutions from the underlying compacting peat. This suggests that the channel was

present during the peat stage, that is, before coalification.

Partings (or very thin dirt bands compared to the surrounding coal) are thin internal

mineral-rich layers or plies in a seam. Partings in seams can originate from various

sources such as volcanic derived materials (gravity-settled ash), wind-transported

detritus or water-borne sediments. The partings in the Sangatta seam consist of

coaly shale (dark in colour) and silty materials (light in colour). Most of the clastic

partings have probably been deposited within the seam through the action of water.

66

Moore (1991) summarised the mechanism of water-transported clastic incursions into

peat swamps as migration or avulsion, flooding and subsidence. Migration or

avulsion would terminate active peat accumulation and erode the top layers of the

peaty. Flooding normally results in deposition of overbank fines and splay deposits

and causes splits in the seam. Rapid subsidence would submerge peat deposits and

they would pass upwards into lacustrine claystone. Clastic partings in the Sangatta

seam may have formed by flooding as both splay and overbank deposits. Evidence

for this includes:

(i) the thickness and grain size of the partings is not uniform, changing

rapidly over a short distance, especially in the eastern area which is

more proximal to the source;

(ii) a crevasse splay deposit, characterised by a thin coarsening-upward unit,

decreases in thickness laterally from D D H F5304 (40 c m ) to C3001

(10 cm); and

(iii) the absence of widely distributed partings.

The positions of partings in vertical seam profiles vary markedly from area to area.

In the western and central areas lower partings are only developed in the west (Fig.

4.3) whereas clastic partings become better developed and more widespread in the

upper part of the seam.

The lower partings consist of LP1 and LP2 (Fig. 4.3). LP1 is a dark brown shaly

coal. This parting is fairly thin (less than 5 c m in thickness) and diminishes to the

east. This probably indicates a distant source for the sediment. L P 2 separates the

lower and upper parts of the lower Sangatta coal bench in the western part of the

67

western area. In drill hole F5304 this parting appears to be a coarsening-upward

siltstone 50 cm thick. The thickness and grain size decrease rapidly toward drill

hole C3001 (10 cm thick). At drillhole C2982, now the E-West Pit, the LP2 parting

is not recognised (Fig. 4.6c). Thus, the thickness and grain size of the LP2 parting

decrease to the southeast suggesting a northwesterly source.

Partings in the upper part of the Sangatta seam are only developed in the eastern

part of the western area where the Sangatta seam is thickest They consist of upper

partings 1 (UP1) and 2 (UP2; Fig. 4.3). In the E-West area, UP1 and UP2 thicken

in both a westerly and easterly direction. UP2 developed into an extensive

interburden unit between the Sangatta and Middle seams in the central, eastern and

northern areas (Fig. 4.8).

In the eastern area, partings vary in thickness and number laterally. At the border

between the central and eastern areas (drill hole C2922) only one thin parting is

developed in the upper portion of the Sangatta seam. The parting does not exist

toward the northwest. However, to the southeast the Sangatta seam contains more

and thicker partings. Figure 4.5 shows that clastic incursions occurred at most levels

in the seam and the materials were sourced from the east. On the southeastern edge

of the study area the Sangatta seam is only recognised as coaly material associated

with shale, siltstone and sandstone. This implies that fluvial sedimentation was

contemporaneous with, and juxtaposed to the east, of the peat swamp.

In the northern coalfield, clastic partings in the Sangatta seam increase in thickness

and intensity toward the north. Farther north, the Sangatta seam is only recognised

as coaly material associated with siltstone and sandstone (Muggeridge, 1987). In this

68

area the accumulation of the Sangatta peat was also terminated by extensive clastic

sedimentation.

The development of clastic partings within the Sangatta seam seems to have been

related to the system of fluvial sedimentation in this area. At least three, and

probably four, channel sand bodies are recognised associated with the Sangatta seam.

1. A channel sand body below the Sangatta seam (Channel A ) was recognised from

lithological and geophysical logs for the western area. The main axis of this channel

is probably located to the west of the western area. Overbank deposits from this

channel have been interpreted as the main source of the parting development in the

bottom part of the Sangatta seam in the western area.

2. A channel in the western part of the study area corresponds to the partings in

the Sangatta seam in the western part of the E-West area (Channel B).

3. A channel sand body complex (Channel C) north of the Hatari Pit was probably

contemporaneous with the Sangatta seam and may have been the main source for the

clastic intervals (partings) within the seam in the eastern area.

4. Several channels above the Sangatta seam are indicated by the presence of

several washout -zones at the top of the Sangatta seam (Channels D ) . These channels

were recorded in the northern, central and eastern areas. In the southern coalfield

these channels probably started with avulsion of the main Channel C to the south.

They are younger than the seam and in some places eroded the top of the seam. In

the central zone, parting development in the upper part of the Sangatta seam may

have been influenced by this system.

Although the Sangatta peat accumulated within the Kutei Basin where the products

of active volcanism have been recorded (Nas and Indratno, 1979; Land and Jones,

1987), widely-distributed volcanic layers have not been recognised in this seam.

69

This may be because the Sangatta peat swamp was not accessible to the volcanic ash

due to a greater distance to the volcanic source. Alternatively, if a raised bog model

is applied, the volcanic materials were probably leached by acidic water as

documented by Ruppert and Moore (1993) in the raised bogs of Sumatra, Indonesia.

In this situation, no discrete partings would be formed.

4.6 SEAM QUALITY DATA

It is known that the geometry of seams, in many cases, is reflected by the chemical

properties of the coal (Ferm and Staub, 1984; Esterle and Ferm, 1986; Cohen et al,

1987). This section documents the vertical and lateral variation of chemical

properties of the coal and attempts to relate these properties to the geometry of the

Sangatta seam. This study is based on numerous analytical data from 1531 coal ply

samples taken from approximately 200 cored drill holes.

Sulphur content

Coal ply samples were analysed for total sulphur content. Three patterns relating to

vertical variation of the sulphur contents from the Sangatta seam are identified (Fig.

4.9). A low sulphur pattern fits the data for the northern and eastern parts of the

southern Sangatta Coalfield (Fig. 4.10). The low values are consistent from the

bottom to the top of the seam with the sulphur content in composite samples in these

areas is also low, normally less than 1%. This is typical for coals originating from

fresh water peat with highly acidic conditions and without brackish water influence at

any stage (Casagrande et al, 1977; Cecil et al, 1980; Cohen et al, 1984, 1989;

Styan and Bustin, 1984; Bustin and Lowe, 1987; Price and Casagrande, 1991; Querol

70

et al, 1991).

To the south the pattern gradually changes to a moderately high sulphur content

(Figs 4.11, 6.59). In this pattern only the uppermost samples of the Sangatta seam

have high sulphur content. This is probably the result of an epigenetic brackish

water incursion at the end of the peat accumulation, as noted in other examples by

Cohen et al. (1983), Casagrande (1987) and Diessel (1992). The brackish water

influenced only the top of the seam.

Along the southern margin of the study area the sulphur content is normally higher

in both the upper and bottom parts of the seam. Although the influence of the high

sulphur content has also extended to the middle of the seam, in this part it is still

within the limit of a low sulphur category since the values are normally less than 1%

(Fig. 4.12). The high sulphur content at the bottom of the seam indicates that the

peat, at the early stage of the development, was effected by brackish water.

Casagrande et al. (1977) suggested a marginal 'marine peat' for the precursor of

this kind of coal. During the period of most intensive peat accumulation, however,

the peat surface was probably slightly elevated, resulting in less effect from the

brackish water in the middle section of the seam. But, during accumulation of the

top part of the seam, the area was again probably influenced by a brackish water

incursion. So, fluctuations in the relative height of the peat surface with respect to

marine influences probably occurred in parts of the Sangatta peat swamp.

Alternatively, structures such as faults or cleats in the seam may have controlled the

concentration of sulphur (and thus pyrite) at the bottom of the seam. A narrow zone

of high sulphur (data from composite samples), located near the Villa Fault in the

71

southern part of the Sangatta Coalfield, supports this hypothesis. However, high

concentrations of epigenetic pyrite in the seam were not recorded from this zone.

In the western part of the Sangatta Coalfield, where the Middle seam merges with

the top of the Sangatta seam, the high sulphur contents are only observed in the

Middle seam portion. Because of the influence of the high sulphur content in the

Middle seam, the very top of the underlying Sangatta seam, in some places, also has

a high sulphur content (because of leaching). A similar feature was documented by

Cohen et al. (1984) for the South Florida peat.

Ash Content

Vertical development of ash yield is comparable with the distribution of clastic

partings within the seam (Fig. 4.10). Five patterns of ash have been recognised.

1. Clean coal, without uniform ash throughout the seam. This is typical for the

Sangatta seam in the western, central and northern parts of the coalfield. In

these areas clastic partings are normally absent from the seam.

2. Elevated ash content near the base of the seam. This, which is typical for the

Sangatta seam in parts of the eastern part of the study area, indicates an

unstable flood-prone swamp at the early stage of peat accumulation.

Interruption may have come from clastic fluvial channels juxtaposed to the peat

swamp.

3. Increase in ash, but only at the top of the seam. This is typical for the

Sangatta seam in the south-central part of the coalfield. The pattern was

influenced by a fluvial system coeval with accumulation of the top part of peat.

4. High ash at the bottom and top of the seam. The accumulation of the peat

72

probably commenced and ended with a low-lying mire in lacustrine conditions.

5. Elevated ash throughout the entire seam (dirty coal). In this situation the

Sangatta seam probably was deposited close to active clastic sedimentation

centred in a contemporaneous fluvial channel. This is typical for the Sangatta

seam in the eastern and far northern parts of the coalfield.

Calorific values and volatile matter

The trend of the calorific values is normally the inverse of the trend of volatile

matter. However, in some cases, mainly in the upper portion of the seam, the

calorific value and volatile matter show similar trends.

Many sections indicate a decrease in calorific values and increase in volatile matter

toward the top of the Sangatta seam (Fig. 4.13). Petrographic details of the plies in

the Sangatta seam (Chapter 5) shows no significant increase in liptinite content

towards the top of the seam, indicating that this is not a liptinite maceral-related

phenomenon.

Thus an alternative hypothesis is needed. A brackish water incursion at the top of

the seam may have caused this relationship. It is known that brackish water

incursions, in most cases, would increase the hydrogen content of the coal (Diessel,

1990, 1992; Davis, 1992; Kuehn and Davis, 1991).

In some places, such trends in calorific values and volatile matter are not apparent.

In a few sections the calorific value increases and the volatile matter decreases

toward the top of the seam. This has probably resulted from a complex interaction

of coal properties, including the maceral composition and the degree of coalification.

73

4.7 COAL SEAM DEPOSITIONAL MODEL (CONCLUSIONS)

The Sangatta seam splits in both the western and eastern parts of the coalfield. To

the west the seam splits into the Lower and Upper Sangatta seams (Fig. 4.8). The

Sangatta seam then thins very rapidly to the west. This splitting was controlled by

clastic sedimentation; abundant sandstone in the same horizon was reported by

Kaltim Prima Coal in the western Melawan Coalfield. Therefore, the tapering of the

Sangatta seam to the west was caused by a lack of peat development due to

extensive clastic interruption.

To the east, the Sangatta seam splits into the Sangatta (lower) and Middle (upper)

seams with a north-trending split line. The split was controlled by different rates of

subsidence with the central area subsiding more rapidly. The lower elevation caused

by the subsidence increased the intensity of clastic sedimentation in the central part

of the coalfield. This is indicated by the thick clastic interval, including channel

sandstone, crevasse splay and overbank deposits, between the Sangatta and Middle

seams in this part of the coalfield.

The Sangatta seam varies in thickness quite markedly. The thickness variation is

probably controlled by several factors including splits, washouts, pinchouts and

probably faults. These factors are believed to be influenced by geological factors

occurring in the peat accumulation setting, such as water table depth, clastic

incursions, differential compaction and channelling (active and abandoned).

The nature of partings within the Sangatta seam strongly suggests a water borne

clastic origin. The deposition of these partings was probably related to a major

74

fluvial system juxtaposed to the peat swamp. The absence of clastic partings in the

western-central part of the coalfield, where the clean coal of the Sangatta seam is

thickest, indicates that this part of the swamp was hardly reached by clastic

sedimentation. The most probable explanation for this is that this part of the peat

swamp must have been elevated above the normal flooding level.

The vertical distribution of some coal quality parameters, such as sulphur, ash,

volatile matter and calorific value, have been found to be related to the geometry of

the Sangatta seam. Specifically, in most of the coalfield the sulphur content tends to

be consistently low throughout the seam, except for the southern-central part of the

study area where the upper and some lower portions of the seam have elevated

sulphur contents. In this zone, the Sangatta peat may have been epigenetically

inundated by brackish water due to more rapid subsidence or greater compaction.

In this study, geophysical logs have proved to be useful for identifying the physical

characteristics of the Sangatta seam and the surrounding clastic strata. Together with

lithology logs this tool has been successfully used to correlate the seam.

75

CHAPTER FIVE

COAL PETROLOGY

5.1 INTRODUCTION

Coal is formed mainly from organic constituents with minor inorganic materials. The

type of coal is mainly determined by the source of organic matter, mode of transport

and the environment of deposition (Smith, 1981).

Coal petrology is the study of type, rank and inorganic matter in coals. In terms of

the environment of deposition, coal petrology is used to explain the initial genesis of

coal macerals and lithotypes.

This chapter describes the petrology of the Sangatta coals and also attempts to

deduce the conditions in the peat-forming environment. Because the Sangatta seam

varies in thickness and quality across the study area, these variations should be

related to the coal facies that can be inferred from the maceral and mineral

associations in the seam (Ferm and Staub, 1984; Esterle and Ferm, 1986).

Numerous outcrops, mine faces and borehole cores and logs were observed to

delineate vertical development of coal-lithotypes in the seam. Fifty drill core coal

samples were analysed microscopically to determine the lateral variations in the

maceral composition and vitrinite reflectance. A n additional forty coal samples,

mostly from mine faces, were analysed to determine the vertical variation within the

seam. Six samples were analysed using Scanning Electron Microscope (SEM) to

76

identify mineral matter in the seam and ash from thirty coal samples were analysed

for trace element contents.

Field observations and the results of petrological and geochemical analyses are used

to discuss aspects of the depositional environment of the Sangatta seam that

influenced seam thickness and quality variation; these variables were used in seam

depositional modelling which is discussed in Chapter 7.

5.2 COAL PETROLOGY TECHNIQUES

Samples for this study were prepared using the procedures described in the Standards

Association of Australia (1986) and International Committee for Coal and Organic

Petrology (ICCP, 1975). The ninety coal samples collected from drill cores, mine

faces and outcrops were crushed, split and set in blocks of polyester resin. A

standard method for sample preparation is outlined in Figure 5.1.

Leitz Orthoplan (MPV1) and Leitz MPV2 Ortholux reflected light microscopes were

used for vitrinite reflectance measurements and maceral analysis respectively. In this

study the classification of the Standards Association of Australia (1986; Table 5.1),

which is based on the maceral terminology of Smith (1981), has been followed.

To reveal the texture of vitrinite group macerals, a number of samples were etched

with a solution of potassium permanganate following the procedures given by Stach

et al. (1982), Moore et al (1990), Quick and Moore (1991), Stanton and Moore

(1991), Moore and Ferm (1992) and Moore and Hilbert (1992) but slightly modified

as outlined in Figure 5.2.

77

Maceral analyses were conducted using the point-counting technique described in the

Standards Association of Australia (1986), ICCP (1975) and Bustin (1991). A

minimum of 400 points were counted in each block. More than 90% of the polished

surface was covered during the point counting. The percentages given in Tables 5.2,

5.3 and 5.4 have been automatically rounded to the nearest 0.1% by the point

counter. This gives a greater accuracy than is real; for a point count of 500 points,

a count of one point in 500 gives a percentage of 02%.

Telovitrinite was chosen for reflectance measurements, because the reflectance of this

maceral is the best indicator of coal rank (ICCP, 1975; Stach, 1982; Bustin et al,

1983; Rimmer, 1991a). The number of readings was decided on the basis of the

standard deviation and confidence interval (Stach et al, 1982; Bustin et al, 1983;

Standard Association of Australia, 1986). Preliminary reflectance studies on the

Sangatta coals, in which the number of reflectance measurement per block was varied

from as few as ten up to 100, showed that the standard deviation of reflectance

measurements in most samples was generally low and 25 points for each block was

calculated as the minimum for a 0.02% reflectance confidence interval (see also

Daulay, 1986).

5.3 COAL FACIES AND THE DEPOSITIONAL ENVIRONMENTS

Coal facies are indicated mainly by the maceral and mineral contents. These are

considered to be the product of initial bio- and geochemical processes on the plant

remains and associated sediments and are influenced by the physical and chemical

conditions in peat swamps. Coal facies have been discussed by several authors such

78

as Smith (1968), Teichmuller and Teichmuller (1982), Neavel (1981), Stach et al

(1982), Diessel (1982, 1986, 1992), Bustin et al. (1983), Hunt and Hobday (1984),

McCabe (1984, 1987), Smyth (1984), Ting (1989) and Calder et al (1991). Most of

these authors suggested that the physical, chemical and microbiological conditions in

peat swamps are predominantly affected by geographic conditions, principally water

depth and related water movement in the swamps. More specifically, Hunt and

Hobday (1984) stated that both local topographic variations and the hydrology of the

peat swamps play important roles in the spatial distribution and generation of coal

facies. Thus the coal facies are intimately related to the depositional environment.

The use of coal facies for interpreting the depositional environments can be assessed

by analysing maceral associations (microlithotypes) and maceral composition in

composite or lithotype samples. The application of microlithotype studies for the

diagnosis of depositional environments has been advocated by authors such as Smith

(1968), Teichmuller and Teichmuller (1982) and Smyth (1980, 1984, 1985). These

authors differentiated the petrographic characteristics, mainly microlithotypes, of coals

according to their sedimentary facies associations. Recently, Mastalerz and Smyth

(1988) correlated coal microlithotypes with the major depositional environments.

Therefore, the palaeoenvironments of coal deposits, as determined by these authors,

was inferred more from the environment of deposition of the associated clastic

sediments than from coal properties. This methodology assumes that the environment

of deposition of coal-bearing strata is always related to the depositional environment

of the coals. Clearly, studies by McCabe (1984, 1987) and Scott (1989) show this is

not always the case.

Furthermore, microlithotype seems to be not always directly related to preservation,

79

degradation and gelification levels of coal macerals, particularly vitrinite group

macerals. Because these levels have been proven to be useful parameters in

interpreting local palaeoenvironmental variations in seams (Diessel, 1985; Calder et

al, 1991; Moore, 1991; Pierce et al 1991), the use of microlithotypes for this

purpose should be supplemented with detailed maceral analysis. This is more time

consuming (Diessel, 1986; Marchioni and Kalkreuth, 1992) but a fruitful exercise.

The use of maceral composition of coal samples for determining peat-forming

environments has been applied by many workers such as Marchioni (1981), Diessel

(1982, 1985, 1986), Harvey and Dillon (1985), Esterle and Ferm (1986), Rimmer and

Davis (1988), Ting (1989), Gentzis and Goodarzi (1990), Calder et al. (1991),

Lamberson et al. (1991), Marchioni and Kalkreuth (1991), Moore (1991), Pierce et

al. (1991) and Strehlau (1991). Most of these studies, show that the conditions in

peat swamps can be deduced from the proportion of oxidised macerals and well-

preserved tissues contained in coals. The degree of oxidation in the coal swamp is

indicated by the inertinite to vitrinite ratio (Neavel, 1981; Harvey and Dillon, 1985),

whereas the level of preservation is characterised by the ratio formulated by Diessel

(1985, 1986): '

telovitrinite (vitrinite A) + fusinite/semifusinite

detrovitrinite (vitrinite B) + gelovitrinite + inertodetrinite + macrinite

A comprehensive study of macerals as palaeoenvironmental indicators was undertaken

by Diessel (1982, 1985, 1986). The concepts of Tissue Preservation Index (TPI) and

Gelification Index (GI) of coals derived from that study were based on the genetic

characteristics of vitrinite and inertinite macerals. Initially, the TP1-GI diagram was

used by Diessel (1986) to distinguish the depositional environment of some

80

Australian coals. He distinguished lower delta plain (marsh), upper delta plain

(terrestrial) and piedmont plain environments. Recently, this model has been widely

used by many workers interpreting the depositional environment of coal deposits

(Lamberson et al 1991; Marchioni and Kalkreuth, 1991; Pierce et al 1991).

The application of the distribution of maceral contents and coal facies in a particular

seam to model peat-forming position in a basin or peat swamp scale has been used

by authors such as Esterle and Ferm (1986), Rimmer and Davis (1988), Marchioni

and Kalkreuth (1991), Moore (1991) and Pierce et al. (1991). These authors have

been successful in distinguishing depositional conditions of various parts of a seam

using maceral contents.

In this study, the Sangatta coal was used to test the coal facies model with facies

mostly delineated on the basis of individual macerals in composite and bench

samples. The diagnostic value of macerals in the three groups (as suggested by

Diessel, 1986) is considered and the facies have been categorised according to

wetness and detrital condition of the maceral precursors. Because the Sangatta seam

is dominantly composed of vitrinite, a detailed study on the macerals of this group

has been undertaken, and the results are discussed according to modern peat

analogues as documented by Anderson (1964, 1983), Anderson and Muller (1975),

Esterle et al. (1989) and Moore and Hilbert (1992).

5.4 MACERAL COMPOSITION OF THE SANGATTA SEAMS

Sangatta coal contains predominantly vitrinite ranging from 84.5% to 95.0% by

volume, with an average content of 91.6% (Table 5.2). Liptinite and inertinite only

81

occur as minor constituents, ranging from 1.2% to 6.1% (3.2% average) and 0.8% to

6.5% (3.1% average) respectively. The consistent lack of petrographic variation in

the three maceral groups is seen in the ternary diagram (Fig. 5.3) which shows that

all data plot near the vitrinite peak, in a very crowded pattern

Vitrinite

Vitrinite consists of telovitrinite (20.0 to 59.5%, average 38.4%), detrovitrinite (27.8

to 67.5%, average of 47.5%) and gelovitrinite (2.2 to 9.7%, average 5.8%). Total

vitrinite contents are normally a unimodal population (Fig. 5.4) but showing

significant variation in the telovitrinite and detrovitrinite contents (Fig. 5.5). This

may indicate a single peat-forming system but one consisting of subenvironments

with significant differences in the morphologic and hydrologic conditions.

In general, two types of telovitrinite are recognisable in most coal samples,

telocollinite and eu-ulminite. Textinite and texto-ulminite are rarely present.

Telocoltinite occurs as discrete 10 to 500 urn homogeneous layers in a detrovitrinite

groundmass (Plate 5.1a) which also commonly contains resinite, suberinite and

cutinite (Plate 5.1b and 5.1c). Occasionally, telocollinite is also found as discrete

large bodies. Observations of the external structures of some telocollinite suggests

that the size of the telocollinite may be origin specific with the different types

having probably originated from different parts of precursor plants, such as root, stem

and leaf mesophyll.

Telocollinite is a product of at least two different processes occurring in the plant

tissue; biochemical and geochemical degradation/gelification. These processes:

82

i) generate gelified materials which mask cell structures;

ii) compress cell structures resulting in very tight cell walls (nearly always

without recognisable cell lumens); and

iii) degrade and destroy the cell walls .

In the maceral description of the Standards Association of Australia (1986), it is

suggested that telocollinite and desmocollinite are mainly produced by vitrinite

metamorphism from eu-ulminite and densinite precursors respectively. Although the

structures of eu-ulminite and densinite are quite different, in m a n y cases, both have

some similar features, for example, both derived from cell wall or cell wall

fragments and commonly associated with gelovitrinite, liptinite and minerals.

Therefore, in some cases, it is not easy to differentiate telocollinite from

desmocollinite without careful observation of the external structures, as also noted in

ICCP (1975). This is due to the difficulty in recognising vitrinitic structure and

texture in the two vitrinite macerals. In addition, the external structures m a y be

destroyed by crushing during preparation.

The occurrence of eu-ulminite is generally similar to telocollinite. The only

difference noted is in the definition of the cell structures where eu-ulminite shows

relatively clear structure. Eu-ulminite generally has compressed and altered cell

structures and the cell lumens are commonly filled with gelovitrinite (mostly

corpogelinite) and resinite (Plate 5.1c).

Microfractures are sometimes well developed in telovitrinite macerals (Plate 5. Id).

Most of the fractures are filled with epigenetic minerals, mainly carbonates. One

83

particular sample, in which telovitrinite is associated with detrovitrinite and

suberinite, clearly shows that the microfractures are preferentially developed in

telovitrinite (Plate 5.4g). This is probably due to differences in physical

characteristics between telovitrinite and detrovitrinite, since the former is composed

of homogeneous, less gelified woody materials. Detrovitrinite comprises more

gelified materials which are more resistant to fracturing.

In terms of microlithotype terminology, most telovitrinite is in liptinite-poor vitrite.

Some telovitrinite, that originated from leaf mesophyll, is associated with quite

abundant resinite (Plate 5.1e) in clarite. Many fractures in telovitrinite are filled with

exsudatinite and this secondary association is found in clarite.

Three detrovitrinite macerals are recognised in most coal samples - attrinite, densinite

and desmocollinite. Densinite and attrinite are mostly associated with liptodetrinite,

sporinite, sclerotinite and syngenetic mineral matter (Plate 5. If). In some samples,

cutinite is 'intercalated' with the attrinitic and densinitic groundmass. Resin bodies

are common in the attrinite and densinite groundmass (Plate 5.1g) and mostly occur

as detrital (probably reworked) bodies in the groundmass. In sample 25011,

densinite is included within semifusinite cell lumens (Plate 5.1h) indicating a more

ductile phase in this degraded vitrinite compared to the semifusinite.

Most desmocollinite appears to be composed of vitrinitic fragments (Plate 5.2a).

This desmocollinite seems to be derived from in-situ degraded woody tissue without

significant associations of other macerals. Some desmocollinite is also believed to

originate from gelified or compacted attrinite and densinite containing liptinite and

inertinite. Thus, detrovitrinite in the Sangatta coal may be differentiated into two

84

groups; detrital detrovitrinite (attrinite and densinite) and in-situ degraded

detrovitrinite (part of desmocollinite).

In terms of microlithotypes, the detrovitrinite macerals mainly occur in liptinite-poor

clarite and vitrinite-rich trimacerite, although in some samples liptinite-rich clarites

are also present. Desmocollinite also occurs in vitrite.

Corpogelinite and eugelinite are the predominant gelovitrinite macerals in the

Sangatta coal with some samples having subordinate porigelinite. Corpogelinite

mostly occurs in vitrinite cell lumens (Plate 5.2b), within suberinite (Plate 5.2c), and

as individual bodies within the detrovitrinite groundmass. In sample 24744, very low

reflecting resinite (with relatively strong fluorescence) is associated with corpogelinite

(with no fluorescence; Plate 5.2d and 5.2e). Eugelinite occurs as an amorphous

matrix (cement) within detrovitrinite.

Gelovitrinite varies in its occurrence and reflectance. This variation could indicate

different chemical compositions for the gelovitrinite macerals but m a y also be due to

different oxidation levels as indicated in the maceral description of the Standards

Association of Australia (1986).

Telovitrinite, detrovitrinite and gelovitrinite show different distribution trends (Fig.

5.6). The bimodal normal population for telovitrinite suggests a bimodal distribution

of the well-preserved plant tissues in the Sangatta seam. The unimodal normal

population of detrovitrinite and gelovitrinite implies that the vitrinite precursors have

experienced a uniform rate of degradation.

85

Liptinite

Liptinite mainly consists of cutinite (0 to 1.7%), sporinite (0 to 1.5%), resinite (0 to

2.2%), suberinite (0.2 to 2.4%), liptodetrinite (0 to 2.0%) and exsudatinite (0 to

4.8%). Cutinite occurs as lamellar bodies with some well-preserved leaf cuticles

(Plate 5.2f) which have a thickness of less than 0.1 urn to 20 um (Plate 5.2g and

5.2h). In some samples leaf resinite is associated with leaf cutinite (Plate 5.1e) as

indicated by the paired forms which were derived from leaves; both top and bottom

cuticles were preserved.

Sporinite is mostly associated with liptodetrinite and inertinite in a detrovitrinite

groundmass (Plate 5. If); some samples contain sporangium. The close association of

sporinite, cutinite and sclerotinite (from cluster analysis; Fig. 5.7) indicates that the

sporinite may have originated from the same flowering broad-leaf, woody plants as

the cutinite, which accumulated as detrital surface litter composed of leaves and

degraded by fungi.

The suberinite appears to be of two forms, either thin or thick structures, both of

which are rarely broken (Plates 5.3a, 5.3b, 5.3c and 5.3d). In some samples, the

waxy nature of the suberinised cell walls suggests they are relatively resistant to

geochemical degradation and this may have acted as an effective shield to minimise

chemical degradation of the woody tissues. The thickness of cork tissue and the

suberinised cell walls may indicate different precursor plants or different plant

tissues. The proportion of broken or fragmented suberinised cell walls suggests that

the intensity of physical breakdown of the tissue was initiated by fracturing due to

exposure of the peat surface before burial.

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According to the cluster analysis (Fig. 5.7), suberinite is in the same group as

semifusinite and liptodetrinite but in microscopic observations this maceral is also

associated with telovitrinite, gelovitrinite and detrovitrinite. The suberinite-

semifusinite association m a y indicate that these two macerals originated from the

outer parts of coal precursor plants. The association of suberinite and liptodetrinite

suggests that m a n y of the liptinitic fragments m a y have been derived from severely

broken suberinite.

Resinite can be categorised into in-situ and detrital bodies. In-situ resinite is the

most c o m m o n form in the Sangatta seam and can be classified into primary resinite

and secondary resinite. Primary resinite originated from resin ducts in the living

plants (for example, woody tissue and leaf mesophyll). This resinite is characterised

by relatively strong fluorescence. Secondary resinite is mostly found in pores,

fractures and bedding planes, and is identified by its irregular shape. The secondary

resinite has similar optical properties to what many refer to as exsudatinite.

However, in Sangatta coal there are two types of organic matter, on the one hand

exsudatinite and- on the other 'secondary resinite' which have properties that grade

from one to the other so that it is difficult to distinguish that which is secondary

resinite and that which is exsudatinite; commonly 'secondary resinite' is associated

with exsudatinite. The association of resinite, exsudatinite and telovitrinite is shown

in the cluster analysis (Fig. 5.7). The fluorescence intensity of the secondary resinite

varies from weak to strong.

Detrital resinite is commonly found in the detrovitrinite groundmass (Plate 5.1g).

The generally relatively weak fluorescence and zoning in some of this resinite

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strongly indicates that the decreased fluorescence intensity (and corresponding

increased reflectance) in the peripheral zones is due to oxidation, a phenomenon also

reported by Stach et al (1982). The detrital resinite bodies are less compacted than

the surrounding detrovitrinite (Plate 5.1g). In samples 24815, 23845, 24734 and

24747, parts of resin bodies have been transformed into fusinitized materials

(micrinite), probably by oxidation or are the residual fractions of disproportionation

reactions that generate liquid hydrocarbons (Plates 5.3e and 5.3f).

In general, primary liptinite macerals (cutinite, sporinite, suberinite) show a lower

fluorescence intensity than secondary liptinite macerals (fluorinite and exsudatinite).

A feature of the resinite, however, is more variable fluorescence intensity than other

liptinite macerals, probably due to the degree of oxidation and metamorphism of the

resinite.

Inertinite

Inertinite consists mostly of fusinite and semifusinite (0 to 5.9%), sclerotinite (0 to

1.0%) and inertodetrinite (0 to 2.4%). Macrinite and micrinite are minor components

in some samples.

In most samples, semifusinite is dominant over fusinite and shows well developed

cellular structure; the cell lumens are mostly empty or filled with mineral matter

(Plate 5.3g). In many samples, the cell walls have collapsed resulting in 'bogen

structures'. Microscopically, semifusinite is commonly associated with detrovitrinite,

but according to the cluster analysis (Fig. 5.7) semifusinite is closely related to

suberinite and liptodetrinite.

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Diessel (1992, p. 59) suggested three modes of semifusinite formation; fusinitization,

fungal attack and incomplete combustion of the same precursors as vitrinite macerals.

In the Sangatta seam, most semifusinite shows well-preserved botanical structures.

However, woody tissues which have 'rays' are commonly recognised in many

telovitrinite macerals of the Sangatta coal (for example, Plates 5.5a, 5.6a, 5.6b) but

were not generally observed in the semifusinite. Although this may be explained by

the effects of physico-chemical modification during oxidation (Stach et al, 1982;

Teichmuller, 1989; Jones et al, 1993) or during the coalification process, careful

microscopic examination indicates that this may not be the case for the Sangatta

seam. An alternative explanation could be that the association may be precursor

dependent, that is, semifusinite and telovitrinite derived from woody tissue probably

originated from different tissues of the same plant or different parts of the same

tissue. Oxidation or fungal attack may have preferentially occurred in the outer parts

of plants or tissues (not woody tissues) or in leaf tissues as pointed out by Jones et

al. (1991) and Diessel (1992, pp. 31, 60-61). The association of semifusinite and

suberinite (Fig. 5.7) supports oxidation of the outer part oxidation of the plant or

plant tissue and this would imply a primary origin of the semifusinite (see

Teichmuller, 1989).

Sharp contacts between semifusinite and the detrovitrinitic matrix, as observed in

most samples, indicates that the semifusinite was not generally affected by the

alteration taking place in the peat swamp. This suggests that semifusinite was

already oxidised before deposition (for example, from burnt vegetation) and,

therefore, this inert material was more resistant to bacterial and/or chemical

decomposition. A similar feature was also reported by Gould and Shibaoka (1980)

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from some Australian coals. It has been suggested that the absence of resinite or

corpogelinite in the semifusinite cell lumens indicates that fusinitization of the cell

walls probably occurred before deposition, possibly in the living plants. This

phenomena was documented by Cohen et al. (1987) in the Everglade peat deposit,

Florida.

This oxidised or fusinitized material (semifusinite and fusinite) would have been hard

to degrade or gelify in the peat swamp and its presence should not necessarily

indicate a high degree of tissue preservation in peat swamps (like suberinite).

Therefore, the role of fusinite and semifusinite in determining the environment of

deposition of seams has to be justified for each and every coal seam. Reservations

when using inertinite macerals as peat-forming palaeoenvironmental indicators has

also been discussed by Mastalerz and Smyth (1988) and Calder et al. (1991).

Sclerotinite occurs as inclusions in telovitrinite and as detrital components in mineral-

rich detrovitrinite (Plate 5.3h). A close relationship between sclerotinite and sporinite

macerals is observed in some coal samples (Plate 5. If). This close association and

similar morphologies of the two macerals indicate that some sclerotinite may have

originated from the same source as sporinite but experienced a different oxidation

intensity, as indicated by ICCP (1975) and Stach et al (1982). This would account

for unilocular sclerotinite with uniform walls but not multilocular sclerotinite

Micrinite and macrinite are rare in the Sangatta seam. Where these occur, micrinite

is commonly associated with liptinite, commonly resinite and this probably indicates

that the micrinite is the residual maceral of liptinite that has undergone

proportionation reactions to generate liquid hydrocarbons, as suggested by

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Teichmuller (1989).

From their occurrence in most samples, inertinite macerals mainly appear to have

been oxidised before peat deposition. Fusinite and semifusinite appear to have been

derived from different types of plant or different organs of the same plant as

telovitrinite precursors. Therefore, the inertinite macerals do not necessarily indicate

good preservation and low gelification in the context of the depositional environment

of the Sangatta seam. Diessel (1992) commented on the role of inertinite in

determining TPI by suggesting that a telovitrinite-based TPI is more reliable in

explaining the loss of biomass in peat accumulation.

Microlithotypes

Transformation of maceral compositional data to produce microlithotype data can be

performed by several formula. Diessel (1992) listed some of the formula used for

N e w South Wales coals as follows:

vitrite = (vitrinite)2/100

clarite = ((vitrinite + liptinite)2/100) - (vitrite)

inertite = 0.55 inertinite

trimacerite = 0.6 (inertinite + liptinite) + 0.05.

Applying the above relationships to the average values of the three maceral groups,

the petrographic composition of the Sangatta coal can be presented as microlithotypes

in the ratios of 82.8% vitrite, 7.1% clarite, 1.7% inertite and 3.8% trimacerite.

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5.5 MINERAL AND TRACE ELEMENTS IN THE SANGATTA SEAM

Mineral contents

The Sangatta seam contains mineral matter ranging in abundance from 0.2% to 3.2%

with an average of 1.9%. Types of mineral matter recognised during the optical

petrographic analyses were clay minerals, carbonates, pyrite and quartz.

In reflected light, clay minerals are observed as dark and cloudy/transparent material

commonly associated with detrovitrinite and also as infillings in cell lumens in

telovitrinite, semifusinite and sclerotinite. The colour varies from black to light grey,

brown, orange and red. Some of the clay minerals have weak fluorescence.

In high-ash coal, clay minerals mainly occur in association with detrital macerals

such as detrovitrinite, sporinite, inertodetrinite and sclerotinite; Plate 5.4a). In

carbonaceous shale samples, clay minerals are frequently associated with telovitrinite

indicating rapid burial of the parent organic matter (Plate 5.4b) and good preservation

of the plant tissue.

Analysis by Scanning Electron Microscope (SEM) of 6 coal samples provided

qualitative identification of clay minerals. Kaolinite is the major clay with minor

Ca-Mg-bearing clay minerals (smectite).

In the study area carbonate occurs as the major mineral component in many coal

samples. Petrographically, the carbonate appears to be transparent, light grey to

brown (with reflection pleochroism) in white light, and non-fluorescing to fluorescing

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in blue light. The colours and fluorescence of carbonate are known to be affected

by the chemical contamination in carbonate minerals (Stach et al, 1982).

Carbonate occurs in both syngenetic and epigenetic modes. Syngenetic carbonate is

commonly observed as detrital inclusions in detrovitrinite (Plate 5.4c) and probably

was introduced into the coal during the peat stage. This carbonate is clearly less

compacted than surrounding macerals. In Sangatta coals, the dolomitic and sideritic

compositions determined by SEM analysis are probably syngenetic minerals which

indicates a marine incursion during peat deposition, as suggested by Stach et al.

(1982). However, many instances of siderite and dolomite occurrence have been

recorded in coaly sequences where a marine incursion is known not to have occurred.

In these instances the formation of sedimentary siderite and dolomite is probably

related to brackish water conditions. Ply-sample geochemical data suggest a brackish

water inundation at the top of the Sangatta peat in some locations.

Epigenetic carbonate, mostly calcite, generally occurs in veins in vitrinite, especially

telovitrinite. Frequently, the carbonate shows fibrous structures (Plate 5.4d). In

some samples, carbonate minerals are closely associated with pyrite in the same

fractures (Plate 5.4e).

Pyrite occurs as a mineral that infills fractures and cavities and is associated with

carbonate in vitrinite and as subhedral inclusions, especially in detrovitrinite. In

detrovitrinite, pyrite is commonly associated with clay minerals, sporinite, sclerotinite

and inertodetrinite (Plate 5.4f). It rarely shows framboidal textures. The distribution

of most framboidal pyrite appears to be controlled more by primary structures of coal

precursors and bedding planes (Plate 5.4h) and is interpreted as syngenetic in origin.

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Trace element contents

Sangatta coals were analysed for the trace elements Pb, Zn, V, As (analysed with

AAS) and Se, Sb, Be (analysed with INNA). The concentration of trace elements in

the Sangatta coal, in general, is relatively low (Table 5.5) compared with the average

figures for coals from other countries given by Swaine (1990).

The Sangatta coal contains 0.3 ppm to 27.7 ppm Pb with an average of 3.4 ppm and

this is lower than the Pb content for most world coals (2.0 ppm to 80.0 ppm). The

Zn contents range is 0.8 ppm to 22.0 ppm (average of 3.9 ppm), and these also are

much lower than typical world ranges of 5 ppm to 300 ppm. As an example, the

typical Zn contents for Australian and European coals cited by Swaine (1990) are

25 ppm and 111 ppm respectively.

Other trace metals contents for the Sangatta coals are:

Vanadium - 0.15 ppm to 13.3 ppm (average of 2.3 ppm) compared to the

Australian and European values of 25 ppm and 60 ppm respectively;

Arsenic - 0.2 ppm to 26.4 ppm (average of 7.3 ppm) compared to values of

0.5 ppm to 80 ppm for other world coals; Australian coals contain lower As

(average of 1.5 ppm) than Sangatta coals.

Selenium and Antimony and Beryllium are extremely low compared to most

world coals.

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The low trace element contents of the Sangatta coal may be a function of the low

ash yields rather than low absolute values of the trace elements. In the Sangatta

coal ash, Pb, Zn, V and As are as high as 176 ppm, 254 ppm, 124 ppm and 498

ppm respectively.

5.6 PETROGRAPHIC ANALYSIS OF ETCHED COAL SAMPLES

The reflectance of most vitrinite macerals in the Sangatta seam fall within the range

of bituminous coals (Rvmax >0.60%). Gelification during peatification (diagenesis)

and coalification has altered the plant tissue morphology and therefore, the structures

seen in the vitrinite are not easy to identify in most cases, a feature also noticed by

Moore and Swanson (1993). To better identify structure in vitrinite, a number of

samples were chemically etched and examined microscopically. This technique has

proven to be useful as after etching structure can be enhanced in many samples thus

revealing variations in vitrinite types that are not seen in unetched samples. Thus a

better understanding of preservation/gelification of tissues is provided and this is

paramount when interpreting depositional environments.

After etching, all liptinite and inertinite macerals and most vitrinite macerals appeared

to be resistant or slightly affected. Eugelinite is the only maceral that is significantly

etched. Because eugelinite is commonly found as an amorphous matrix (cement) in

detrovitrinite and as a mask in telovitrinite, the black colour of etched eugelinite has

provided clear evidence of structures in vitrinite macerals. With this technique,

recognition of the preservation level of botanical structures in vitrinite is enhanced.

Eight different types of vitrinite (excluding eugelinite) have been recognised during

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the microscopic analysis. According to the ICCP (1975) and Stach et al. (1982) the

terminology for each maceral should be prefixed with 'crypto'. For simplicity,

however, in this study this prefix is not used.

1. Very well-preserved woody tissue. This tissue still shows intact clearly defined

woody structures consisting of tracheid cell walls, parenchyma rays and vessel

elements either in tangential or cross-sections. Many of the structures are

comparable with modern woody plants from Sarawak (Plate 5.6) and those described

by Esau (1962) and Martawijaya et al. (1986). This comparison suggests that most

of the precursor plants for the Sangatta coal were angiosperms. The cells have thin

and thick walls occasionally showing primary and secondary growth. Vessel

elements and parenchyma rays are clearly distinguished. Some of the tissue has been

compressed and some cell walls are very rigid.

Based on comparisons with modem wood structures from Sarawak and the

morphology and coalification of woody tissue as discussed by Esau (1962),

Martawijaya et al. (1986) and Shearer and Moore (1992), the woody tissues in the

well preserved vitrinite were probably derived from angiosperm and gymnosperm

woods. Angiosperm wood is characterised by thin fibre tracheids, multiseriate rays

and well-developed vessels (Esau, 1962; Moore and Swanson, 1993). The vessels

and parenchyma rays are mostly replaced by gelified material and are now

recognised as corpogelinite (Plates 5.5a, 5.6b). Gymnosperm wood, on the other

hand, usually has thick dense tracheids with uni or biseriate rays (Plate 5.5b). The

rays are replaced by corpogelinite and occasionally by resinite.

According to some authors cell walls of angiosperm wood contain less lignin

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compared to gymnosperm wood, and thus the former is relatively easily attacked by

fungi (Stout and Spademan, 1989). Shearer and Moore (1992) reported that lignin in

angiosperm wood is composed of syringyl and guaiacyl whereas gymnosperm wood

has more guaiacyl and is more resistant. Hatcher et al. (1987) pointed out that

angiosperm lignin is composed only of syringyl causing the wood to be less resistant.

Diessel (1992) mentioned that gymnosperm wood is often resinous and resistant to

aerobic decomposition. Therefore, with respect to the same peat swamp condition

gymnosperm woods would have a greater preservation potential.

Well-preserved woody tissue was probably derived from relatively resistant material

(perhaps containing more lignin) which was subject to very good preservation

conditions and did not experience significant gelification. This type of woody tissue

was said to be equivalent to 'telinite' by Esterle et al. (1989) and Moore and Ferm

(1992). In unetched samples, this maceral could be textinite, texto-ulminite, eu-

ulminite or telocollinite as defined by the Standards Association of Australia (1986).

2. Moderately well-preserved woody tissue. Parts of the ceU walls have been

altered by in-situ degradation (Plate 5.5c) and with 500x magnification only parts of

the cell structures are still recognised. This type of vitrinite is termed 'degratelinite'

and may be equivalent to the 'post-telinitic' maceral of the Institute of Geology of

Academy of Science of the USSR, Moscow (IGM) discussed in ICCP (1975).

3. In-situ altered/degraded tissue. Most fragments have been derived from

altered/degraded and broken cell wall tissues without any significant displacement

(Plate 5.5d). The original orientations of the cell wall fragments are, sometimes, still

recognised. This type of vitrinite is termed 'detrotelinite' (Esterle et al, 1989) and

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may be equivalent to 'precollinitic' maceral of IGM discussed in ICCP (1975).

4. Physico-chemically altered/degraded tissue. Most of the original tissues or

vitrinitic fragments are not recognised and have experienced significant displacement

(physical breakdown). The fragments are commonly associated with an extensive

amorphous matrix (eugelinite), liptinite and inertinite components (Plate 5.5d). This

type of vitrinite is classified as 'vitrodetrinite' and may be equivalent to 'collinitic'

and 'leiptinitic' macerals of IGM discussed in ICCP (1975).

5. Well-preserved corpogelinite and porigelinite. This vitrinite includes intact

corpogelinite within fresh and altered cell walls of associated telinite and

corpogelinite within a vitrodetrinite groundmass. Corpogelinite (up to 200 |j,m)

appears to be the most resistant maceral during the etching process (Plate 5.5f) and

probably originated mainly from gelified material of living plant cell walls (Esau,

1962; Teichmuller, 1982; Cohen et al, 1987). Esau (1962) suggested that extensive

development of this material in woody vessels may indicate a deficiency of water in

the plants. This type of vitrinite is classified as 'corpogelinite' and 'porigelinite'.

In some samples, well-preserved corpogelinite is still well oriented within intensively

decomposed tracheid cells and in tangential sections other corpogelinite appears to be

well-preserved structureless bands between fibre tracheid cell walls. This indicates

that corpogelinite, in most samples, is better preserved than the associated telinite.

6. Gelovitrinite in suberinite. Although this is also resistant to etching, the

occurrence and morphology of this gelovitrinite is different to corpogelinite. This

vitrinite which is closely associated with suberinised cell walls commonly which form

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structured cork tissue (Plate 5.5g). The well-preserved cork tissues are probably the

result of this association. This type of gelovitrinite has been separated from telinite

or corpogelinite and described as cork tissue (some of it is from roots). It has been

classified as phlobaphinite (Teichmuller, 1982). Using the maceral description

terminology of the Standards Association of Australia (1986), m u c h of the structured

phlobaphinite that is seen in etched samples, would be included in telovitrinite if it

was viewed only in unetched samples because the structure is only revealed with

etching.

7. Leaf vascular tissue. These are commonly rimmed with cutinite and

occasionally associated with leaf resinite. The cell walls are commonly very thin.

This vitrinite is termed 'phyllovitrinite' (ICCP, 1975; Stach et al, 1982) but in the

Standards Association of Australia (1986) it would be placed in telovitrinite.

8. Undifferentiated tissue. Although this vitrinite is moderately well-preserved and

shows well-defined plant structures, the origin of these tissues is not clear. Moore

and Hilbert (1992) suggested that this type of material is referred to as macerated

tissue.

Based on the results of the etched coal samples (Table 5.4), vitrinite in the Sangatta

coal comprises an average 13.4% telinite (range of 3.5 to 27.2%), 15.0% degratelinite

(7.6 to 29.9%), 25.0% detrovitrinite (10.0 to 40.0%), 39.1% vitrodetrinite (22.7 to

53.0%), 0.5% corpogelinite/porigelinite (0.0 to 1.7%), 3.2% phlobaphinite (0.4 to

7.4%), 1.0% phyllovitrinite (0.0 to 0.8%) and 3.3% undifferentiated tissues (1.0 to

8.5%; Fig. 5.8a).

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Examination of the etched samples show that the variation and trends in the vitrinite

composition are not as constant as indicated by standard petrographic analysis of

unetched samples. For example, telinite derived from preserved angiosperm wood

comprises 6.9% and varies from 0.2 to 25.8% of the vitrinite macerals. This

indicates reasonable variation of preservation conditions and distribution of types of

vegetation within the Sangatta peat swamp.

Regarding subgroups, the vitrinite comprises 28.5% (15.0 to 53.3%) telovitrinite

(telinite plus degratelinite), 64.2% (41.6 to 79.9%) detrovitrinite (detrotelinite plus

vitrodetrinite) and 7.3% other vitrinite (Fig. 5.8b). These data indicate that the

percentage of telovitrinite obtained from etched samples is lower than that from

standard petrographic analysis using unetched samples. This is because much of the

cork, phyllovitrinite and undifferentiated tissues, which is included in telovitrinite in

standard maceral analysis, would be separated from the telovitrinite after etching;

structure is clearly recognisable. Therefore, this vitrinite should be included in the

telovitrinite subgroup because it clearly shows structure.

The etching technique used in this study provided better resolution of the botanical

structures of vitrinite macerals and enhanced comparisons with modern plant tissues.

Most of the botanical structures found in the Sangatta coal are directly comparable

with the modern plants from Sarawak (Plate 5.6; samples from Dr Joan Esterle) and

Kalimantan (Martawijaya et al, 1986). Furthermore, this technique has provided a

better understanding for the application of the term 'woody' tissue in coal macerals.

Wood almost always has a set of rays (Moore, pers. comm., 1993). The use of

vitrinite derived from woody tissue to assess preservation and degradation conditions

is thought to provide a better result, than is given by unetched samples, because each

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type of plant tissues has different preservation/degradation characteristics during the

peatification (van der Heijden et al, 1994).

5.7 LATERAL PETROLOGICAL VARIATIONS OF THE SANGATTA SEAM

Petrological characteristics of the Sangatta seam vary across the study area. Because

the seam is dominantly composed of vitrinite, the variation is better observed in the

vitrinite maceral contents. However, variation in the occurrence and abundance of

accessory macerals and mineral matter are also observed.

Although it is not a clear pattern, total vitrinite content is slightly higher in the

middle of the southern coalfield (Surya Pit) and increases slightly to the southeast,

changing from 92% to 95% (Fig. 5.9a). Liptinite and inertinite show a

corresponding decrease. First order trend surface maps (Fig. 5.9b) shows that

liptinite content decreases slightly to the east, from 3.6% to 2.8%, and inertinite

content decreases to the southeast, from 4.5% to 2.5%. Mineral matter tends to be

slightly higher in the centre of the coalfield and shows an increase to the southeast,

from 1.5% to 2.1%.

Lateral variations in vitrinite macerals are indicated from both standard petrographic

analysis and from etched sample analysis. The results of standard analyses show that

detrovitrinite is more dominant in the centre of the Sangatta Coalfield compared to

the western and eastern areas. In the central area, however, the detrovitrinite

macerals commonly lack a detrital appearance and these are thought to be mainly

derived from in-situ degraded peat. In comparison, in the western and eastern areas,

detrovitrinite is commonly associated with detrital components such as sporinite,

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sclerotinite, inertodetrinite, clay minerals and an extensive amorphous eugelinite

matrix. Telovitrinite contents, generally, are higher in the western and eastern areas,

typically greater than 40%, than in the central part of the coalfield (Fig. 5.13a).

Clearer patterns of variations and trends are obtained from the etched vitrinite

analyses. Telovitrinite (telinite + degratelinite) is more abundant in the western area

(>30%) where the Sangatta seam merges with the Middle seam (Fig. 5.10a). In the

central area (Surya Pit) where the Sangatta seam splits, the telovitrinite content

decreases to <30%. Telinite content shows a clear pattern (Fig. 5.10b), with >10%

in the west and east, and <10% in the centre of the coalfield. A clear trend is also

shown by variations in the contents of angiosperm wood (Fig. 5.13b) and cork tissue

(Fig. 5.12a). Vitrodetrinite content is highest in the centre of the coalfield and

decreases dramatically toward the western area (Fig. 5.11b).

The lateral variation in the type and abundance of vitrinite is thought to indicate the

lateral changes both in types of precursor vegetation and preservation-degradation

conditions during peat deposition. In addition, the variation in the structure of

detrovitrinite submacerals is assumed to be the result of differences in the intensity

of physical breakdown. These conditions are probably related to the local

topography and water regimes of the peat-forming swamp.

The data also show a variation in the degree of preservation of cutinite in the study

area. Well-preserved cutinite mostly occurs in coal from the eastern area. Because

cutinite is highly resistant to chemical and bacterial attack and the degree of

preservation is probably related to the climatic weathering conditions (Stach et al,

1982) with the intensity of weathering which in turn is probably related to the depth

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of water in the peat swamp.

Fusinite and semifusinite are more abundant in the western area. This may have

resulted from more intensive oxidation due to a shallow or fluctuating water level or,

alternatively, from a different type of vegetation. Inertodetrinite and sclerotinite are

more abundant in the eastern area than in the western area and a similar relationship

is also observed for the distribution of sporinite. This m a y indicate a greater level

of physical breakdown or transportation of the organic precursors in the eastern area.

In the western area of the Sangatta Coalfield the inorganic components are

commonly clay minerals, epigenetic pyrite and carbonate, whereas in the eastern area,

most of mineral matter is detrital clay minerals, syngenetic dolomitic/sideritic

carbonate and syngenetic pyrite (occasionally framboidal pyrite). This probably

indicates changes in the water regime from shallow, stagnant and acid in the western

area to deeper, flowing and more neutral waters in the eastern area.

5.8 VERTICAL VARIATIONS IN LITHOTYPES

In hand specimen or outcrop, the Sangatta coal is generally bright reflecting the

abundance of vitrinite and minor inertinite and liptinite. However, careful

observations of drill core and mine faces indicate thin (<5 m m ) super bright bands in

the bright coal. The abundance of super bright bands varies from the bottom to the

top of the seam and is probably related to the variation of maceral composition. The

vertical development of the maceral composition seems to vary from place to place

across the Sangatta seam.

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In the western part of the Sangatta Coalfield, the abundance of the super bright

bands generally tends to decrease in the middle of the seam for example, drill hole

F5304 (Fig. 5.14). At this locality, this tendency is observed in both the lower and

upper splits of the Sangatta seam. Moore and Ferm (1988, 1992) and Esterle et al

(1992) showed that the abundance of super bright bands correlates with the presence

of xylite in other Tertiary Indonesian coals and thus it is assumed that in the western

part of the Sangatta Coalfield the proportion of xylite decreases in the middle as

well. This suggests that a less woody peat developed in the middle of the seam,

or alternatively, the preservation of the middle peat was relatively poor.

In the central part of the Sangatta Coalfield, no significant trend is observed in

vitrinite maceral composition (for example, drill hole C3536; Fig. 5.15). However,

confirmation of the vertical variation by etching coal samples from this drill hole

indicates a trend of an upward decrease in the telinite content. In this area, inertinite

content increases slightly toward the top of the seam. The decreased telinite and

increased inertinite contents toward the top of the seam may be the result of drier

conditions and also the type of woody vegetation in the peat swamp environment.

In the eastern part of the coalfield, an upward increase in telovitrinite content is

observed in a few of the upper coal samples (for example, Fig. 5.16). In this area,

inertinite also tends to be higher in the upper samples except for the uppermost

sample where the inertinite content slightly decreases. The increased telovitrinite

may have been caused by rapid burial of the peat by fine-grained clastic sediments.

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5.9 VITRINITE REFLECTANCE OF THE SANGATTA SEAM

Vitrinite reflectance is one of the best parameters for measuring the degree of

coalification or rank of coals. Rank is a function of the geothermal gradient and

burial-depth history.

Vitrinite reflectance is largely related to the aromaticity of the vitrinite which

increases with increasing rank. The environment of peat formation influences the

level of preservation and oxidation of organic matter and also, to some extent,

contributes to the initial development of vitrinite aromaticity (Teichmuller and

Teichmuller, 1982; Titheridge, 1988; Cohen and Rich, 1991; Kuehn and Davis, 1991;

Rimmer, 1991a). Peat accumulated under the influence of marine or brackish water

is slightly lower in aromaticity, and thus shows a decrease in the reflectance of the

resultant coal.

Permeability and conductivity of roof rocks have been considered to be factors that

control heat expulsion and heat transfer to the roof (Pearson and Murchison, 1990).

Coal rank decreases slightly where permeability and conductivity of the roof rock is

high. Similarly, liptinite content was also found to be negatively correlated with

vitrinite reflectance, a phenomenon also found by Raymond and Murchison, 1991).

Hutton and Cook, 1980 and other authors found that increased telalginite (derived

from Botryococcus) content also decreases vitrinite reflectance.

The vitrinite reflectance of the Sangatta coal ranges from 0.58% to 0.71% with an

average of 0.66%. The coefficient of variation of reflectance data within samples

(5.4%) is slightly higher than that between locations (4.9%). This may indicate, in

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general, the influence of oxidation during peat accumulation (Cohen and Rich, 1991).

Comparing the rank of Sangatta coal with the stages of coalification, and parameters

for determining rank, as proposed by Teichmuller and Teichmuller (1982), the rank

of the Sangatta coal, based on vitrinite reflectance is slightly higher than the rank

expected where it is based on dried ash free volatile matter content. However, the

rank based on vitrinite reflectance is lower than expected for the rank defined by the

moist mineral matter free calorific values (Fig. 5.17). This is probably related to the

high vitrinite plus liptinite to inertinite ratio in the coal since the former macerals

have higher in calorific values (Stach et al, 1982).

Vitrinite reflectance and, therefore, rank gradually increases from west to east,

however it is laterally more variable in the western area (Fig. 5.18a). In this area,

the variability of reflectance data within samples is also higher (Fig. 5.18b) than in

the eastern area. This may suggest that the western area was exposed to greater

variations in the levels of oxidation (see Cohen and Rich, 1991).

In the study area, the increase in reflectance could have been caused by an increase

in the geothermal gradient and the depth of burial. The eastern area has a higher

heat flow due to deeper burial, because it was closer to the basin depocentre (Fig.

2.3) where sediment were thicker. The position of the seam relative to the Makassar

Strait spreading centre (Miocene), is also considered to be another factor influencing

the increase in vitrinite reflectance because active spreading centres frequently have

an increased heat flow regime. However, a study of several coal rank parameters

(moisture, calorific value, volatile matter) from the three main seams (Sangatta,

Middle and Pinang seams) indicates a post- or syn-tectonic coalification. Therefore,

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the depth of burial and geothermal gradient influenced by the Pinang D o m e

diapirism, a post- or syn-tectonic event, may have been the major factor determining

the trend of in the rank (and therefore vitrinite reflectance) in the Sangatta seam.

This is consistent with the regional pattern of reflectance distribution verified from

first order trend surface analysis which indicates a gradual increase toward the

Pinang Dome.

The problem with this interpretation, however, is that the increase in the reflectance

values is not constant. The vitrinite reflectance rapidly increases from the west to

the middle of the study area, whereas from the middle to the eastern area the

increase is less marked (Fig. 5.18a). Since there is no significant difference in the

roof lithology or liptinite content of the Sangatta seam throughout the coalfield, the

lower rate of the increase may have been influenced mainly by the initial conditions

within the peat-forming environment.

It has been suggested that the western area had been exposed to greater oxidation,

whereas the central and eastern areas are associated with very wet conditions. The

different oxidation and water level conditions may have influenced the chemical

characteristics of peat in the two areas which, in turn, determined the initial rank

development in the peat swamp (Cohen et al, 1987; Cohen and Rich, 1991; Kuehn

and Davis, 1991; Diessel, 1992). The initial rank of coal was probably slightly

lower in the eastern area and this may have been responsible for decreasing the rate

of increase in the vitrinite reflectance. Similar trends in reflectance have been

observed in reflectance of Late Cretaceous Menefee and Crevasse Canyon coals in

the San Juan Basin of N e w Mexico by Cohen and Rich (1991).

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5.10 DISCUSSION AND SUMMARY

Sangatta coal has abundant vitrinite and this indicates that the coal originated in a

wet forest swamp environment (Teichmuller and Teichmuller, 1982; Bustin et al,

1983) mainly from arborescent vegetation (Rimmer and Davis, 1988). The high

content of degraded vitrinite (as a general characteristic) in the Sangatta coal may

have resulted from a greater degree of degradation of woody tissue, mainly

influenced by the type of vegetation, depth of water, pH, bacterial activity,

temperature of peat (Teichmuller and Teichmuller, 1982; Stout and Spackman, 1989;

Titheridge, 1988; Shearer and Moore, 1992) or by mixed environmental conditions

across the peat swamp (Marchioni and Kalkreuth, 1991).

Assessment of the depositional environment using Gelification and Tissue

Preservation Indices (Diessel, 1986), however, have placed the Sangatta seam in a

'marsh' environment with a treeless vegetation (Fig. 5.19). This is quite

understandable since this coal contains little telovitrinite and very small amounts of

inertinite. These macerals are the major determinants for TPI and GI. However, the

very low ash yield and sulphur content does not support this interpretation, since

'marsh' coals normally have high ash and sulphur contents (Diessel, 1986; Scott,

1989).

Because of the low ash, sulphur and inertinite contents, the depositional environment

of the Sangatta seam is believed to have been a very wet raised bog system, as also

suggested by Diessel (1992, written pers. comm.). The significant amounts of woody

tissues in many coal samples indicate that the raised bog was partly occupied by

arborescent vegetation. The dominance of vitrite lithotype in most coal samples

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suggests that the raised bog occurred in a fluvial sedimentary system (Smyth, 1984,

1985) and this is also consistent with the sedimentological data.

With respect to modern analogues, most tropical raised bogs in the Indo-Malaysian

region contain woody vegetation (mainly angiosperms) with a low ratio (<1) of

preserved to degraded woody material (Esterle et al, 1989, 1992). Plotting the

petrological data of peat from the Indo-Malaysian raised bogs (Crosdale, 1993) on

Diessel's TPI7GI diagram suggests that those data also fall within a woodless 'marsh'

environment. Crosdale argued that this was wrong as it is for the plots of Sangatta

coal. Therefore, the application of the original form of Diessel's TPI/GI diagram for

interpreting depositional environments of raised bog coals seems to be inappropriate

for Sangatta coals for several reasons:

a) low diagnostic value of detrovitrinite submacerals (Diessel, 1982, 1986;

Marchioni and Kalkreuth, 1991);

b) non-diagnostic macerals (mostly detrovitrinite) comprise more than half

of the total maceral content in seams (Marchioni and Kalkreuth, 1991);

c) low inertinite and very high vitrinite content would apparently indicate

very high gelification index; and

d) more importantly, the TPI/GI diagram was established especially for low

moor coals from Australia which have much higher ranks (Diessel,

1992, written pers. comm.).

Preservation Degradation Ratio (PDR) of coal macerals, a modified form of Diessel's

TPI, was applied by Pierce et al. (1991) to assist in determining the environment of

deposition of the Lucerne #9 seam from west-central Pennsylvania (USA). These

authors formulated the P D R as the ratio of telinite, semifusinite and fusinite to

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gelovitrinite and macrinite. Although the use of etched samples in this study resulted

in a better identification of vitrinite macerals, the PDR still uses similar parameters

to Diessel's TPI. Furthermore, in the Pierce et al. model, the types of gelovitrinite

are not clearly determined and inertinite macerals are still taken to indicate high

preservation and low gelification levels. Therefore, on the PDR diagram, Sangatta

coals will give similar misplaced plots. Again this would be an erroneous conclusion

if accepted unquestionably.

Although the tissue preservation and gelification concept is believed to be an

excellent tool for determining environments of deposition for many coals, for the

Sangatta seam, it should be used with some discretion. In order to obtain better

results the following modifications should be made:

a) tissue preservation levels should be based only on telinite or well-

defined woody cell tissue as revealed with etched samples which show

that different parts of plants would give different

preservation/degradation characteristics (Waksman and Stevens, 1929, in

Diessel, 1992, p. 18; van der Heijden et al, 1994);

b) fusinite/semifusinite do not necessarily be used to indicate excellent

preservation (Calder et al, 1991);

c) inertinite does not be necessarily to indicate a low gelification level

(Calder et al, 1991);

d) gelification levels should be based on the intensity of primary

gelification in detrovitrinite (or the proportion of eugelinite in vitrinite);

and, if possible,

e) wood type should be used to estimate preservation and gelification

levels, since woody tissues from different plants would give different

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preservation properties (for example, Stout and Spackman, 1989; Diessel,

1992; Shearer and Moore, 1992).

However, since the concept of gelification is still not well established (Diessel, 1992,

p. 180; Crosdale, 1993) due to the difficulty in differentiating gelification generations

using optical methods, in this study, it is not used to determine the conditions in

environments of peat deposition.

The local variations in the depositional environment of the Sangatta seam were

largely determined using the tissue preservation and degradation levels. The variation

of telinite and vitrodetrinite contents were extensively examined. T o confine the type

of tissues used in this examination, only woody components were counted as telinite

whereas well-preserved cork and leaf tissues have been excluded because of the

different preservation and degradation characteristics of wood versus cork and leaf

tissue (White, 1925; Cook, 1982; Phillips and DiMichele, 1990; Diessel, 1992).

Petrographic evidence for local zoning in parts of a seam have been interpreted as

suggesting that the precursor peat has accumulated in a raised bog environment

(Anderson, 1983; Cameron et al, 1989; Scott, 1989; Esterle et al, 1989; Calvert et

al, 1991). In the Sangatta seam, however, clear zoning is only observed in vitrinite

composition. This may be related to the origin and preservation/degradation

conditions of vitrinite precursors.

With respect to the environment of deposition, a high detrovitrinite content generally

indicates a high water level with a neutral p H or high bacterial activity (Teichmuller,

1982) or lack of woody plants (Diessel, 1982, 1985) in the peat-forming

Ill

environment. Coals with high detrovitrinite contents also have high hydrogen

contents and/or volatile matter (Brown et al, 1964; Cook, 1982). For the Sangatta

seam, localities where detrovitrinite content in high (middle part of the study area)

may be interpreted as having a high rate of subsidence and open water. These have

been interpreted as the margins of low-lying parts of the peat swamp system which

were undergoing continuous subsidence.

However, the Sangatta coal from this area has a low volatile content. The decrease

in volatile matter is probably related to deeper burial. Alternatively, low volatile

matter content in the high detrovitrinite coal is probably due to the degradation of

the vitrinite precursors under the influence of oxidation (controlled by aerobic

decomposers) as indicated by Diessel (1985), and postulated by Newman (1989) and

Shearer (1990) for some New Zealand coal deposits. If this is the case, the central

area of the coalfield should be interpreted as the centre of a raised bog where the

water level was low and thus oxidation was greater. High detrovitrinite content may

also have resulted from non-woody herbaceous precursor plants (Diessel, 1982, 1985;

Warwick and Stanton, 1991) which were a function of a low nutrient in the area.

Telovitrinite is mostly derived from woody tissues that has undergone minor

gelification. Thus telovitrinite is interpreted as having formed within an environment

with a low pH and low bacterial activity. However, the abundance of this maceral is

also controlled by the population of woody tissues in the peat swamp (Diessel,

1985).

The observed increase in telovitrinite in the western area of the coalfield indicates

that the area was probably the highest part of the peat swamp with a low stagnant

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water level (acid water). It could be the centre of a high moor peat. This

interpretation is supported by the relatively low total vitrinite contents (Esterle and

Ferm, 1986). The higher initial reflectance of vitrinite precursors, as assumed earlier

in this chapter, indicates a slightly higher degree of oxidation. The high variability

of the telovitrinite reflectance in the western area also indicates complex oxidation

resulting from fluctuations of the water table at the centre of the raised bog where

water was mainly supplied by rain.

A high telovitrinite content which is also observed in parts of the eastern area where

the Sangatta seam is split could be explained through a rapid burial of the peat as

suggested by Rimmer and Davis (1988). In this area, peat may have been

immediately covered by clastic sediment, therefore, decreasing the opportunity for

bacterial activity to decompose woody tissue. However, only the southeastern part of

this area contains significant clay partings indicating periodic clastic sediment

incursions. Petrographic analysis also indicates an increase in mineral content of the

coal in the southeastern part of the study area.

Alternatively, the observed increase in telovitrinite in the western area and parts of

the eastern areas of the coalfield indicates extensive growth of woody plants with a

low level of degradation. These areas were probably near the margin of a raised bog

where water was deeper and where oxidation was inhibited and nutrient supply was

high. This is also indicated by the higher content of well-preserved angiosperm

woody tissue in the coal. In the eastern area, however, telovitrinite and angiosperm

woody tissue contents are lower. This suggests that this area was frequently

disturbed by clastic sediment deposition, the sediments of which later became the

partings in the seam in this area; the development of woody plants was inhibited.

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Higher pH levels increased bacterial activities, which in turn increased decomposition

levels in the area.

Concentration of angiosperm wood in the western area and parts of the eastern areas

infers at least two environmental possibilities:

(a) angiosperm vegetation was only concentrated in these areas; or, alternatively,

(b) because of good preservation conditions in these areas, angiosperm woods were

preserved.

The strong trend showing cork tissue content decreasing from east to west indicates

that plants with well developed bark tissue were less developed in the western area.

Alternatively, this result shows a westward decrease in the root/shoot ratio.

Irrespective of which hypothesis is correct, the western area was probably dominated

by angiosperm woody vegetation (trees) with a low root/shoot ratio (Diessel, 1992,

p. 179) and low proportion of cork tissue, whereas the central area was dominated by

stunted vegetation with a high cork tissue content (probably derived from a high

root/shoot ratio).

The mineral content of the Sangatta coal also shows a gradual increase to the

southeast. The abundance of mineral matter in the southeastern part of the study

area suggests that the peat swamp was significantly influenced by clastic sediment

incursions. This may be interpreted as a low-lying part of the peat swamp that was

probably close to the influx clastic sediments. In the western area, mineral matter

occurs mainly as disseminated and epigenetic minerals associated with coal macerals.

The lack of detrital mineral matter in this locality indicates it was probably away

from, or higher than, normal flood water levels.

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The petrological variation in Sangatta coal suggests that four different peat forming

environments existed during accumulation of the Sangatta seam (Figs 5.20, 5.21).

1. The western area (E-West Block) has been interpreted as the margin of a raised

bog in which the peat comprised abundant woody angiosperms that gave rise to

a coal characterised by a high telinite content.

2. The central area (Surya Block) is assigned to the centre of the raised bog

which was characterised by a lack woody angiosperm. The coals have little

telinite but abundant detrovitrinite which has a low hydrogen content. The

central area subsided relatively rapidly in the final stage of peat accumulation

as indicated by the high sulphur and volatile contents at the top of the seam.

3. The eastern area or Hatari Block has been interpreted as a low-lying part of the

raised bog as indicated by the high mineral content of the coal. High telinite

derived from angiosperm woody tissue indicates that arborescent vegetation

occupied parts of this area.

4. Although only few petrographic data are available for the northern area (C-

North and C-South Blocks), the depositional environment appears to be have

been similar to that for the eastern area.

Etching a number of coal samples provided a better identification of vitrinite types

and this has proven to be beneficial when examining local variation in petrographic

composition of the Sangatta seam. The data have been used, successfully, to

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interpret local variations in palaeoenvironments of the seam. Furthermore, it is

suggested that when studying aspects of environments of deposition of any coal

samples composed chiefly of vitrinite and with a vitrinite reflectance above 0.5%, the

etching technique should be considered an important part of the study (see also Scott,

1991). However, the identification of detrovitrinite derived from cork tissues,

including the suberinised cell wall fragments and gelified humic materials, is

accomplished best using unetched samples. Consequently, for studies on the

environments of deposition for Sangatta coals, and probably for most Indonesian

coals, a combination of etched and unetched samples should be used. Following on

from this, use of the Standards Association of Australia (1986) nomenclature or the

ICCP nomenclature for macerals is not suitable for palaeoenvironmental

interpretations because they do accommodate structured and gelified vitrinite as

revealed by etching samples.

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117

CHAPTER SIX

STATISTICAL PARAMETERS OF THE SANGATTA SEAM

6.1 INTRODUCTION

The statistical analysis of several seam parameters, obtained from field measurements

and laboratory work during the exploration stage in the Sangatta Coalfield, was

undertaken to evaluate systematically the spatial variation of each parameter. It was

also used to reveal the spatial relationship between the parameters across the

coalfield. These are the basic steps when formulating a genetic geological model to

explain the spatial distribution and variation of the coal thickness and quality

parameters. The variability should be partly explained by the environment existing

during the formation of the seam and partly by post-depositional processes.

Mostly, the statistical analysis in this thesis has used original data from the

exploration program. The data were collected from drill hole information, including

the coordinates and values of each coal parameter. However, in special cases, data

manipulation, including log transformation and averaging of the data, has been

employed.

This chapter describes the results obtained from the statistical analysis of the coal

parameter data, including thickness, ash content, sulphur content, type of sulphur,

moisture content, calorific value, volatile matter content, ultimate analytical and ash

composition data. Descriptions are separated into three parts: data collection and

preparation, methodology consisting of basic and spatial statistics and results of the

statistical analysis. The results are described separately for each parameter.

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6.2 DATA COLLECTION AND PREPARATION

Data were recorded from 209 core holes (spacing approximately 200 m) and 1718

combination holes (spacing approximately 100 m , Fig. 6.1) and stored in an ASCII

database system. The computer program Brief 3.0 was used to set and format the

data, and Microsoft Excel 4.0 and QuatroPro for Windows 1.0 were used in some

transformations and conversions. Four main data files were generated from the drill

hole records for statistical analysis:

1. Combination hole data (1718 drill holes) contain thickness records, X-Y

coordinates, collar, and top and bottom depths for each hole (Appendix

6.5). Seam elevations (structure) were calculated from the collar and

depth using Microsoft Excel 4.0. The statistical features of thickness

and structure were delineated mainly from this data set. This large data

set was also separated into several subsets according to the geographic

blocks using computer program LIMIT (Appendix 6.1).

2. Cored-hole data from 209 holes provided thickness records and 169

holes provided composite ash content and composite sulphur content

records (Appendix 6.6).

3. Weighted average ply sample data were derived from 1531 records

(Appendix 6.7) in 167 cored holes, each of which contained ash content

and sulphur data. Averaging for each drill hole was conducted using

the computer program QuatroPro for Windows 1.0.

4. Coal rank data from 147 cored holes contained volatile matter, calorific

value and moisture content records. All volatile content and calorific

value data were converted to dry ash free basis using Microsoft Excel

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4.0.

5. Ultimate analysis, ash composition and form of sulphur data from 83

cored holes (Appendix 6.8) contained C, H, O, S and N contents (from

ultimate analysis), A1203, Fe203, Ti02, K20, MgO, CaO, C02, P205

Mn204, NajO and S03 contents (from ash composition analysis) and

pyritic, sulphate and organic sulphur content (from form of sulphur

analysis).

6.3 STATISTICAL METHODS

6.3.1 Basic Statistics

Basic statistics for each coal parameter are mainly displayed through histograms and

probability curves. The histograms display the geometrical distribution of the data

according to appropriate classes and the proportion of these classes within the data.

The histograms are used to indicate modality, normality, spread and outliers in the

coal data.

The linearity and the slope of probability graphs of the classed values should indicate

the normality and variability of the data respectively. Kinks on the graphs also

indicate the number of populations from which the data were derived and in turn,

give an indication of the uniformity of the depositional environment for mineral

deposits (Rendu, 1985). Rendu also showed a relationship between probability

graphs and types of mineral deposits.

In the Sangatta seam the histograms and probability graphs are used to explore the

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univariate structures of the distribution in the coal data. From the diagrams, it is

seen that the thickness data are distributed normally in two populations, while quality

parameter data show positively skewed distribution in one population.

The mean, median, standard deviation, variance, skewness and kurtosis are the

descriptive statistics displayed with the histogram. They determine the average or

mid value and the spread of the data about the mean. The summary of the basic

statistics for each coal parameter are tabulated in Table 6.1.

Because the magnitude of each coal parameter is quite different, to compare the

degree of variability among the coal parameters (thickness, ash content, sulphur

content, moisture content, calorific value and volatile matter) the coefficient of

variation was obtained by dividing the standard deviation by the mean. Together

with the skewness values, the coefficient of variation are used to confirm the

normality of the data distribution as discussed by Koch and Link (1971). They

stated that data with more than 0.5 coefficient of variation cannot be a normal

population, whereas those much less than 0.5 m a y be, but are not necessarily,

normal. Shaw (1961, in Rock, 1989) indicated that a value of 0.2 for the coefficient

of variation was generally the border between normal and lognormal populations.

For the Sangatta seam only the thickness data, with a coefficient of variation less

than 0.5, shows a clear normal distribution.

To explore the relationships between the values from some coal parameters,

scatterplots have been drawn. The degree of correlation obtained from regression

analysis, in fact, indicates that many of the coal parameters are not correlated with

each other. Therefore, in the case of the Sangatta seam, this statistical method is not

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adequate for analysing most coal parameters to extract meaningful information for

geological interpretation.

6.3.2 Spatial Statistics

The coal parameter data set contains values which are areally distributed over the

Sangatta Coalfield. The values for the mean and the variability change from place to

place across the area. Their distributions are not discrete, but the values are

dependent on each other as a function of distance. The use of ordinary statistics to

analyse these types of data does not consider spatial context, and it is not adequate

for evaluating areally-distributed data (Howarth, 1983). For example, it is shown

later in this chapter that statistically-uncorrelated data are not necessarily uncorrelated

in the spatial context. Therefore, in order to understand the spatial statistical features

of the data (for example, quantitative spatial dependencies), some spatial statistical

methods have been applied. They include Q-mode cluster analysis, geostatistical

analysis, trend surface analysis and moving windows statistical analysis. All of these

methods consider the locations of the samples as a major factor in their statistical

analysis.

Q-mode Cluster Analysis

Q-mode cluster analysis reveals whether the data were collected from groups

distributed within different clustered locations; it is also able to determine if the data

are collected from a single population or from mixed or different populations (Davis,

1986). Although Q-mode cluster analysis can be used to assess spatial distribution of

various parameters, it is not really a spatial statistical technique because in its

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calculations the locations are not regarded as a statistical variable.

A cluster analysis program developed by Dr B. G. Jones (University of Wollongong,

N S W , Australia) in Fortran-L77 based on the Cormat/Prob computer program (Jones

and Facer, 1982) was used in this cluster analysis. Cosine theta correlation

coefficients (see Table 6.2 for the formula) were used to measure the similarity of

coal parameters among the locations. Because the magnitude of each parameter is

significantly different, the program standardised the data to have a zero mean and

unit standard deviation. This standardisation also enables the data to be plotted

together on the same x-y cartesian system (for example, Fig. 6.2).

Cluster analysis using the six parameters (thickness, ash content, volatile matter, rank,

sulphur content and moisture content) revealed 3 groups of data. The data for the

first and second groups are randomly distributed mainly in the eastern, middle and

southern parts of the Sangatta Coalfield (Fig. 6.3). The data for the third group are

clustered mainly in the western part of the area. Statistical elements for each group

are presented in Table 6.3. From this table, it can be seen that the highest mean of

thickness, ash content and moisture content values are in group 3. For sulphur

content and rank, the highest values of the mean are located in group 1. Group 3

has the highest variability for the ash content, sulphur content and moisture content

For the thickness data the highest variability occurs in group 2.

Cluster analysis using three parameters, thickness, ash content and sulphur content

reveals 4 groups. Data from group 1 and group 2 are distributed randomly in the

western, middle and eastern parts of the coalfield, whereas data from groups 3 and 4

are mostly distributed in the eastern part of the area (Fig. 6.4). The statistical

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elements of each group (Table 6.4) show that the means of the thickness, sulphur

content and moisture content are highest in groups 1 and 2, whereas the mean ash

content is highest in groups 3 and 4. The coefficient of variation of the thickness is

low in groups 1 and 2. However, these two groups have a high coefficient of

variation for the ash content and sulphur content.

The results of the Q-mode cluster analysis indicate that the distribution and

association of the coal parameters is not distinctly defined. Although they can be

clustered into western and eastern groups, they also appear mixed within these

locations. This is probably caused by the lack of correlation between coal

parameters. Alternatively, this may have resulted from the properties of the Q-mode

cluster analysis in which only positive relationships are considered in grouping the

samples.

Geostatistical Analysis

One of the major problems in evaluating areally-distributed geological data is to

quantify the degree of spatial continuity or variability of the data across the area

studied. The variogram, one of the most important tools in geostatistics, has been

proved to be a useful tool for determining the degree of such a spatial continuity

(Knudsen and Kim, 1987). Rendu and Ready (1982) and Hohn and Neal (1986)

showed the interrelation between quantitative elements obtained from a variogram and

the geological features, particularly the degree of continuity of mineral or

sedimentary deposits.

The variogram analysis has been developed using the concept of Regionalised

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Variables (Matheron, 1963). This concept assumes most earth science data can be

considered as regionalised variables whose spatial dependencies are determined by

their geographical position. Within a certain variable, a sample value must be related

to other samples; the degree of the relation is a function of the distance and

orientation between samples. The variogram determines the degree of dependence

and the rate of change of a Regionalised Variable along a specific orientation (David,

1977; Journel and Huijbregts, 1978; Clark, 1979; Armstrong, 1981; Rendu and

Ready, 1982; Davis, 1986; Knudsen and Kim, 1987; David, 1988; Hohn, 1988;

Isaaks and Srivastava, 1989; Hester and Springett, 1990; Kim, 1991; Brooker, 1991).

In the early stages of the development of variogram analysis, this method was used

mainly by mining geologists to solve the uncertainty in reserve estimation problems.

As the geology in most mining areas is usually already well defined, modelling the

variograms has usually been guided by the known geology. In other words, in mine

planning phases, geology has been widely used in modelling variograms.

Recently the variogram analysis method has been applied to other branches of

geological science. For example, Rendu and Ready (1982) illustrated a relationship

between variograms and geological environment in several areas, Hohn (1988) and

Hohn and Neal (1986) demonstrated the anisotropic features of variograms related to

the structure of a basin in Virginia, USA, and Camisani-Calzolari (1987) used

variogram analysis to interpret spatial continuity of hydrogeochemical parameters in

the northwestern Cape area, South Africa. Later, Whateley (1991) recognised the

spatial structures of coal thickness data in the Leicestershire Coalfield, England, by

using variogram analysis. Liu (1992) used variogram analysis to characterise the

dimension and areal distribution of thickness variation in the Carboniferous coal-

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bearing rocks of southeastern Kentucky. More recently, Weerts and Bierkens (1993)

showed that different types of overbank deposits in the Rhine-Meuse delta complex,

The Netherlands, had different thickness variability reflected by their variograms. In

these cases, variogram analyses, contributed to the interpretation of geology in

specific areas.

Practically, variograms are simply x-y plots of distances versus variogram values

(Fig. 6.5). The variogram values are calculated on the basis of one-half the mean

squared difference between paired samples according to the specific distance between

sample points. This basic concept is formulated as follows:

2N «=i

where, y(h) is the variogram value at the specific distance h (lag);

Zj and Z ^ are the values of a Regionalised Variable at point i and i+h

respectively;

N is the number of pairs used in the variogram computation.

In multivariate statistical terms, the variogram would be a mirror image of the

autocovariance of the variable.

The lags and number of pairs are two components which commonly control the

reliability of the result of a variogram computation (Knudsen and Kim, 1987; Isaaks

and Srivastava, 1989). Shorter lags provide higher rehability, but usually decrease

the number of pairs, which also reduces the reliability. Therefore, in the case of a

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small number of samples, a compromise is needed when deciding the number of lags

and the number of pairs to be used. As a general guidance, the lags should be about

the same spacing as the data points and the minimum number of pairs should be

approximately 30 (Knudsen and Kim, 1987; Isaaks and Srivastava, 1989). In

directional variogram analysis, the angle of tolerance has to be chosen where the data

points are not regularly distributed. Smaller tolerance provides a more reliable result

when seeking the range of anisotropy. Choosing optimum lags and tolerances, with

adequate pairs in order to produce a clearly structured variogram (meaningful

variogram), is trial and error work and is termed variogram experimentation (>90%

of geostatistical work, Baafi, pers. comm.). The results are experimental variograms.

As in any x-y graphics, the experimental variograms readily provide values for the

variogram y(/i)with the given distance (h). In most geostatistical studies, however,

the variogram values need to be "positive definite"; that is, within the range area, the

values of the variogram have to continuously increase with the distance. To obtain

such values, the experimental variograms must be fitted to an adequate model to

enable them to be use in Kriging calculations. Several variogram models have been

proposed by geostatisticians, such as spherical, Gaussian, deWijsian, exponential and

linear models. The spherical model is the most common and best-defined model

used in analysing geological data (David, 1977; Journel and Huijbregts, 1978;

Knudsen and Kim, 1987; Hohn, 1988; Isaaks and Srivastava, 1989; Brooker, 1991).

Three major parameters determined by a spherical modelled variogram are the nugget

effect, sill and range. Theoretically, the variogram values at zero distance must be

zero. In fact, many variograms have a value at h = 0 called the nugget effect.

This is due to the very erratic nature of regionalised variables over short distances

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(Davis, 1986). The sill is the value where the variogram levels off; it should be

approximately equivalent to the variance of all the data used in the variogram

development (David, 1977; Knudsen and Kim, 1987; Brooker, 1991), although in

some situations this may not be the case (Barnes, 1991). The range is the distance

at which the variogram levels off. It indicates the degree of dependence between

samples within a specific support (David, 1977; Journel and Huijbregts, 1978; Clark,

1979; Davis, 1986 and Knudsen and Kim, 1987). Thus the range is simply the

traditional geological notion of the range of influence (Armstrong, 1981; Knudsen

and Kim, 1987). Beyond the range, the samples are no longer correlated.

In this study, geostatistical analysis was used to determine the structural

characteristics of the thickness and quality data of the Sangatta seam.

Omnidirectional and directional variograms have been applied to reveal the features

of spatial continuity and variability of the coal data.

In the variogram analysis, one omnidirectional and eight directional variograms (at

22^° spacing) were computed and the results are presented through the graphics of

7(/z)-distance (for-example, Fig. 6.5). The computer programs GAM (slightly modified

from Knudsen and Kim, 1987), RGAM (Kim, 1991) and GEO-EAS 1.2.1 (Englund

and Sparks, 1991) were used in the variogram computations. RGAM is an updated

version of GAM and provides the computation of a relative variogram, but it needs

more running time. Ordinary variograms were mainly calculated by GAM. The

GEO-EAS is an interactive program but it has a limited number of data entry points

and pairs; the maximum data points and pairs that can be run in this program are

1000 and 16000 respectively. Modelling and cross-validation of variograms can be

undertaken interactively in this program. Because of the data entry limitation, the

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G E O - E A S was mainly used for variogram computations of cored data sets which

have approximately 200 data points.

Various lags and tolerances have been examined in this geostatistical study. The

clearest results, in terms of the variogram parameters and the isotropy, have been

produced from data with 50 and 100 m lags and 15° tolerances. T o obtain better

variogram structures, various techniques were applied such as filtering, transforming

and smoothing the data and separating the data according to their geological

conditions. From the experimentations, the following features could be drawn:

1. In the E-West area, filtering the extreme values from the thickness data

did not improve the variogram structures. For the Surya (Central) area,

this technique provided clearer structures in the variograms.

2. In the eastern area, filtering the extreme values of the thickness data

increased the range in omnidirectional variograms and increased the

degree of isotropy in directional variograms. In the eastern area, the

anisotropy may have been caused by thinning of the seam.

3. The sill values of the variograms are not always necessarily equivalent

to the variance of the samples.

4. For the whole area, smoothing the thickness data using spatial moving

window statistics provided clearer variogram structures, clearer large

scale anisotropy and reduced the nugget effect although it exaggerated

the range values.

The large number of closely-distributed thickness data points permitted

numerous experiments in variography and this permitted the examination

of small- and large-scale variabilities.

5.

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The clearest variograms from each data set were chosen to be fitted mostly with the

spherical model. Computer modelling was used in GEO-EAS generated variograms,

whereas free hand technique was applied to modelling GAM generated variograms.

Although the two techniques use similar concepts, the model from the computer is

better defined by a mathematical equation as follows:

y(h)= 5///*[1.5(^-0.5(^)3]^^^ h < a

y(h)= sill —*—> h > a

where h is the distance and a is the range value. The sill and range were chosen

to fit the experimental variograms. In the free hand technique, a straight line is

drawn approximating the first few points in the experimental variograms intersecting

the line of the sill. The range is defined as 1.5 times the horizontal distance

between the origin and the intersection point (David, 1977). The values of modelled

variogram parameters are tabulated in Table 6.5. Generally, from the range values it

can be seen that most coal parameters indicate directional anisotropic features in their

continuity.

In some situations, experimental variograms are not readily fitted to the theoretical

models due the erratic behaviour. In these situations, trial and error modelling

should be undertaken to search for the best model. Cross-validation is one of the

techniques used to choose the best variogram models whose parameters (nugget

effect, sill and range) provide optimal conditions when used in a point kriging

process. A comprehensive process of cross-validation is referred to by Kim (1991)

who suggested some criteria to be used when deciding acceptable variogram models;

130

in kriging results the mean errors, error variance and kriging variance should be

minimum.

Moving Window Statistical Analysis

Moving window statistical analysis is an analysis undertaken in a series of small

windows created by splitting a geological area into a number of equally sized areas

(windows: Isaaks and Srivastava, 1989). The windows can be justified according to

their positions (overlap or not, moving windows) and their sizes. In a computer

program developed in this thesis (WIND; Appendix 6.2) the shape of the windows is

optional; rectangular and spherical were used (Fig. 6.5a).

Statistical parameters are calculated from the data within each window including

mean, standard deviation, variance and coefficient of variation. The results are

assigned to the centre of each window and are contoured to provide moving window

maps.

The moving window maps of mean values display local variations of averaged values

of each coal parameter which may aid in the interpretation of regional and local

trends. Moving window maps of standard deviation and coefficient of variation

values show changes in the local variability of the coal parameters across the

coalfield. Through the moving window maps, relatively high and low value areas

can be separated. Similarly, areas with greater variation can be distinguished from

more uniform areas. The trends obtained from moving window maps of averaged

values are used to check the results of the trend surface analysis.

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In addition, the statistical parameters (mean, standard deviation and coefficient of

variation) from each window were plotted on x-y scatterplots to check the

proportional effect of the data. This technique also provides randomisation of

clustered data distributions by placing averaged values obtained from the clustered

points at the centre of each window. The randomised data can then be processed

with variogram or trend surface analysis.

The mechanism of moving is controlled by the width of the windows and the

increments for the centre. The width defines the number of data points within each

window; the increment determines the number of windows. In the case of small data

sets, a compromise between the width and increment resulted in overlap between

adjoining windows. For window statistics, a variation of 100x100 to 1000x1000 m

windows and 100 to 500 m increments were analysed. Where necessary, overlapped

areas were limited to 50%. The minimum number of points allowed in each window

was five; below that statistical calculations were skipped and no value was assigned

to the centre point

From the moving window statistical experiments, several features were noticed:

1. 100x100 m rectangular windows with 100 m increments provided too

many points and unsmoothed maps. The resulting data were used in

variogram and trend surface analyses.

2. 1000x1000 m rectangular windows with 500 m increments provides too

few points and over-smoothed maps.

3. 400x400 m rectangular windows with 200 m increments provided the

most useful data for the moving window statistical analysis.

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4. Because no correlation existed between the number of data points and

the mean, standard deviation and coefficient of variation, the minimum

of 5 points in each window is considered to be adequate for the

statistical analysis.

Trend Surface Analysis

Trend surface analysis is a multiple regression analysis commonly applied in geology,

that is, it is the statistical method most commonly used to minimise the sum of

squared differences between observed and predicted values by using a least square

technique. In this study, the predicted values for the coal parameters are a function

of their X and Y coordinates and can be calculated by the following regression

equation (Ripley, 1981; Balch and Thompson, 1989): n n-k

k=0 ;=0

where, A is the regression coefficient

n is the degree of the polynomial.

Mathematical solution of the trend surface analysis is principally to find the

regression coefficients. This consists of matrix setting and computation. The

predicted values (trend values) at each data location where the coordinates are known

were calculated using these coefficients. Trend values were also computed for grided

points and were contoured by contour programs. All calculations, statistical tests and

griding were computed using a program TREND (Appendix 6.3).

Trend surface analysis has been recognised as a valid technique and has been used

by several workers to study the pattern of spatial variation of geological data (for

133

example, Krumbein, 1959; Cook, 1969; Davis, 1986). Cook (1969), Cook and

Johnson (1975), Cook (1978) and Jakeman (1980) used the technique to evaluate

spatial variation of several coal parameters in the Sydney Basin, Australia. Kantsler

et al. (1978) used trend surface analysis to clarify the pattern of lateral variation of

organic maturation in the Bass and Gippsland Basins, Australia. Smith and Cook

(1984) used the technique to delineate burial depth in the Gippsland Basin.

Recently, Rimmer and Davis (1988) and Rimmer (1991b) use the trend surface

technique to outline the variation of coal quality and petrological data in the Lower

Kitaning seam, Pennsylvania.

The main objective of using trend surface analysis in this study was to separate

spatial coal parameter data into two components, that is, a regional trend (regional

variation) and a residual value (local variation or local noise), to evaluate the data

more easily. In this study, trend surface analysis was carried out from low to higher

order trends. The best fit and the most significant trend surfaces were determined on

the basis of the statistical R2 and F tests respectively. However, because statistical

significance tests are not always necessarily valid for the best geological

interpretation (Davis, 1986), geological conditions were also considered when

choosing meaningful trend surfaces.

One of the major problems encountered when applying the trend surface technique

was clustering of the original data point distribution (Harbaugh and Meriam, 1968;

Doveton and Parsley, 1970). Harbaugh and Meriam (1968) recommended a

randomised sampling technique using small windows to decluster the control points.

However, choosing representative data for each window is still subjective. In the

case of the Sangatta Coalfield, the spacing of drill holes in southern area is much

134

closer than in the northern area. Therefore, in order to use randomly distributed

data, the author used either of the computer programs R A N D O M (Appendix 6.4) or

W I N D (Appendix 6.3) to choose a value or to assign an average value to each

window; the average value was then used in the trend surface analysis.

Trend surface analysis was also undertaken in several blocks of the Sangatta

Coalfield. The main reason for doing this was to confirm the local trends and local

regularity of the coal parameters across the coalfield (which had already been

deduced from geological observations). Furthermore, trend surface analysis from

1000x1000 m blocks was run and the estimated values in the centre of the blocks

were contoured to show general patterns of the coal parameters.

The results of statistical calculations of the trend surface analysis are attached in

Table 6.6 and the geological interpretations are discussed below, separately, for each

coal parameter.

6.4 RESULTS OF THE STATISTICAL ANALYSIS

The results of the statistical analysis are described for each coal parameter, for

example, thickness, ash content, sulphur content, moisture content and rank data.

Each discussion commences with the basic statistical results (Table 6.1) and

summarises the spatial variation of the coal parameter.

6.4.1 Thickness data

The basic statistical parameters were obtained from analysing the combination and

135

cored-hole data. One of the most significant observations arising from the basic

statistics is the tendency towards normal bimodality and unimodality for combination

hole data and cored-hole data respectively (Fig. 6.6). This is because the cored holes

were placed mainly in the prospective locations, resulting in less spread and less

variable values, whereas the combination holes recorded both prospective and

marginal thickness values. The marginal values form a separate normal population

with an average thickness of approximately 2.5 m compared to the main population

which has an average thickness of 6.5 m.

Alternatively, this difference in modality may represent the different borehole

spacings in the two sets of data; the closer data points (combination holes) have

greater possibility of recording the extremely low to extremely high values. If this is

the case, this statistical feature should indicate a complex variation in the seam

thickness. The two normal populations of thickness data may indicate that the

thickness has been developed in two stages; the initial stage was controlled by

environmental conditions within the peat swamp and the second stage was a

modification of the thickness mainly by washouts and faults. The unimodal normal

population in the E-West sub-area and the bimodal normal populations in the Surya

and Hatari sub-areas (eastern area) may further indicate that in the E-West area the

thickness was not significantly modified. This interpretation is confirmed by the

recorded distribution of washout zones on the top of the Sangatta seam which mostly

occur in the eastern areas.

The distribution of thickness was initially represented by an isopach map indicating

no clear pattern, except for a faint north-trending, thick zone that appears in the

western part of the southern Sangatta Coalfield (Fig. 6.7). A clearer pattern was

136

given by the contour map produced from the moving average data. In the southern

coalfield, the average value contour map (Fig. 6.8) shows a clear north-south trend

for the thickness; in the E-West area the Sangatta seam thins gradually from 9 m to

1.5 m westward and from 9 m to 4 m eastward. This pattern becomes more distinct

with the third order trend surface map on which the thickest zone tends to be located

in the central area of the coalfield (Fig. 6.9). The positive residual in the E-West

area surrounded by the negative residual areas on the western and eastern sides, is

still concordant with the moving average map.

The results of trend surface analysis based on the data from the southern coalfield

show a similar trend (Fig. 6.10). The first order trend surface map, although it has a

low fit, indicates the tendency of the Sangatta seam to be thicker in the south (Fig.

6.11). The third order trend surface map indicates a tendency for thickening in the

seam toward the central part. However, the negative residuals suggest that the

thickness in this part has been modified probably by flooding, washouts or faulting.

This is probably because this area has subsided more rapidly (Chapter 4).

The thickness variability changes from place to place across the coalfield. A zone

with more uniform thickness located in the E-West area has a coefficient of variation

less than 0.3 but grades to zones with more erratic thickness on the western and

eastern sides (Fig. 6.8b). The moving window statistics indicate a negative

correlation for thickness between the local means and coefficients of variations (Fig.

6.12). Thus, there is a spatial difference in data variability from each window where

the thicker parts of the seam have lower variability. The scatter plot between the

local mean thickness and the corresponding standard deviation shows no correlation

indicating no proportional effect in the thickness distribution (Fig. 6.12b).

137

Further study of the thickness variability using variogram analysis indicates that the

thickness of the Sangatta seam shows quite marked spatially variability. The

omnidirectional variogram for all data has a 420 m range indicating quite a low

degree of continuity (Fig. 6.13). The high slope of the variogram below the range

indicates a high rate of the thickness change over a short distance, which is also

confirmed by the h-scattergram with a 50 m distance (Fig. 6.14). The presence of a

nugget effect in the typical thickness variogram also implies that the thickness is

quite erratic near the origin.

However, kinks in the omnidirectional variogram may indicate a nested structure

where the thickness has various scales of range such as short and long distance

ranges and trends (Fig. 6.13). This set of ranges may be influenced by the trend of

one particular orientation in the directional variograms (for example, a southeast

direction).

The directional variograms have various values of range in the eight directions

(Table 6.5) indicating an anisotropy of the thickness distribution. The variograms

from four main directions are shown in Fig. 6.15 where the longest range (580 m,

that is, the best continuity of thickness), is in the southeast direction (135° direction).

The anisotropic feature becomes more distinct in directional variograms from

randomised or smoothed data (Fig. 6.16) where the thickness is most continuous to

the southeast (135°) indicating a good trend. However, in the southeast direction the

thickness data show a nested structure with local 'noise' indicated by the nugget

effect in the variogram.

138

Zonal anisotropy is a typical feature in the thickness directional variograms where

different ranges exist with the different sills. The nested structure shown by the

omnidirectional variogram m a y also reflect the zonal anisotropy because one can

separate two different sills in the same variogram, although Whateley (1991) used the

nested structure obtained from the coal thickness variogram as a geometric

anisotropy. Zonal anisotropy is commonly encountered in earth science data (Isaaks

and Srivastava, 1989).

The thickness distribution may have been controlled by the environmental conditions

during the peat formation as well as the processes taking place after the deposition.

T w o different conditions developed during Sangatta peat formation, as mentioned in

Chapter 4, and these are indicated by the results of basic statistics and Q-mode

cluster analysis. The thickest part of the seam in the western area of the southern

coalfield m a y reflect a coal formed in a raised bog environment where the

accumulation of peat occurred without significant clastic influx. The major process

taking place after deposition was only compaction, resulting in a relatively uniform

thickness. Variation was caused only by the different thickness from the centre to

the margin of the bog. Also, the low degree of variability is indicated by the small

nugget effect and high range in the variogram. The weak anisotropy of the

directional variograms may indicate that sedimentary controls were not significant in

this area.

In the eastern area, the seam is thinner and more variable. Here, the thickness

distribution and variability may have been controlled by both the peat-forming

conditions and post-depositional processes. In this area the peat probably

accumulated not far from clastic sedimentary activity. Therefore the formation of

139

peat was quite frequently disturbed by muddy flood water. Because subsidence was

greater in this region, parts of the peat were eroded, as indicated by several washout

zones at the top of the seam. Together with syn- or post-depositional faults, the

washouts have modified the thickness resulting in higher spatial variability in the

data. The pattern of the faults and washout zones may have influenced the

anisotropic direction of the thickness data.

The anisotropic orientation (with the most continuous thickness in a southeast

direction) of the thickness data over the whole area is probably a manifestation of

the major depositional sedimentary setting in the Sangatta Coalfield. The major

channels in the fluvial system generally flowed in a southeast direction (Chapter 3)

and probably controlled the lateral development of peat as pointed out by Home et

al. (1979), Hobday (1987) and Esterle and Ferm (1993). These authors suggested

coal (peat) that developed in fluviatile and upper deltaic environments would be more

continuous in the depositional dip direction. The large scale changes and trends in

the thickness, in this direction, were mainly controlled by the north-trending seam

split line. The split caused substantial change in seam thickness distribution where

the unsplit seam' (western part) is thicker than the split seam (eastern).

In the southern coalfield, the direction of the thickness continuity changes in the

central and eastern areas; the most continuous distribution is in a north-south

direction. This was probably influenced by the presence of crevasse channels (some

with washouts) and faults mostly trending in a north-south direction. The crevasse

may have been sourced from a south bank avulsion from the main southeasterly

flowing river.

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6.4.2 Ash content

The statistical parameters of ash content data of composite samples differ

significantly from those of ply sample data (Table 6.1). The most significant

differences are the means, types of populations and the variability. Ash content from

composite samples has a smaller mean (2.2%) and indicates a unimodal positively

skewed distribution (Fig. 6.17) whereas ash content from ply samples has a higher

mean (6.4%) and a bimodal distribution (Fig. 6.18). The data range and coefficient

of variation are also higher for the ply sample data. The two types of data are not

correlated statistically (Fig. 6.19).

The higher ash content of the ply samples is due to incorporating mineral matter

from clay bands thicker than 5 cm in the data; the latter were excluded from the

composite samples. The ash content values of the ply samples thus reflect the

number and thickness of inorganic partings in the seam. Lack of correlation between

the two types of ash content data was probably the result of different sampling

methods. Geologically, this may indicate different controls in their formation. The

composite ash was controlled by the occurrence of both dispersed inorganic materials

(including inherent organic ash) and thin partings, whereas the ply ash was strongly

influenced by the development of discrete clay bands in the seam. This is also

indicated by the unimodality in the composite ash data and bimodality in the ply ash

distribution. In the ply ash, the smaller and larger mean populations may indicate

the influence of dispersed and discrete inorganic origins respectively.

The lateral distribution of ash content data is highly variable as shown by the

contour map (Fig. 6.20). The spatial irregularity of the ash content values is

indicated by the low multiple correlation coefficient and low significance values of

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the trend surface analysis. However, the ply ash has a better fit indicating a more

significant pattern on the trend surface (Fig. 6.21).

The ply ash content tends to increase in a northeasterly direction from 2% to 11%,

as shown by the first order trend surface map (Fig. 6.21a). A similar trend is also

indicated by the moving average map (Fig. 6.22a). However, the ash values in the

western area, in general, tend to be relatively low. This trend may be related to a

clastic supply from the central north where the main river flowed to the southeast

The gradual decrease in ash content to the southwest may reflect a decrease in the

number and thickness of partings in the seam, and this is a function of the distance

from the river to the peat swamp.

A good correlation between the local means and standard deviation of the ash

content data obtained from moving window statistics, indicates a proportional effect

(zonation) in the spatial distribution (Fig. 6.23a). The standard deviation tends to

increase in the central and eastern parts of the coalfield as the local means increase.

The zonation may indicate that clastic sediments did not reach the western part of

the peat bog, whereas the eastern part was frequently influenced by flooding and

crevasse splays. These processes were recorded in the Hatari Pit where flooding and

crevasse splay deposits were commonly found. The increased variability of ply ash

content to the east may be explained by the irregularity of parting thickness in this

area. The partings were deposited by crevasse splays which spread into the peat

swamp and the size of the crevasse splays influenced the thickness of the partings so

that larger crevasse splays gave rise to thicker partings. The seam thickness

variability now reflects the parting thickness variability.

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The composite ash content tends to increase eastward from 1 % to 2.6%. The

distribution is more variable in the eastern part (Fig. 6.24). The spatial distribution

also shows a proportional effect indicating a slight zonation in the composite ash

distribution. This suggests that the clastic partings have influenced the composite ash

content, although not as extensively as the ply ash.

An omnidirectional experimental variogram, from the original data, indicates that the

ash content data are spatially distributed quite irregularly. However, a variogram

calculated from the logarithm data show a clearer structure with 0.1%2 nugget effect,

0.28%2 sill and 600 m range. A calculation of the smoothed data manipulated by

moving window statistics provides the best-defined variograms for the ash content

data (Fig. 6.25b), although the variogram parameters have been modified by the

technique. For example, if the nugget effect is significantly reduced and approaches

a zero value as the range increases to 800 m. The variograms from the two

manipulated data sets, especially from the smoothed data, have been used to search

for anisotropic features in the ash distribution.

The high spatial variability of the ash data is probably the result of a complex

mixture of inorganic materials in the seam. For the ply ash, the high variability can

be explained by a high variability in parting thickness. This is understandable

because most of the partings were deposited by water from a fluvial system. The

variability was probably exaggerated by the occurrences of crevasse and splay

channel deposits as observed in the Hatari Pit.

Directional variograms from the smoothed data reveal an anisotropy in the ash

distribution. The anisotropy is more characterised by the different sill and range

values; thus this is sill and range anisotropy (Zimmerman, 1993) or zonal anisotropy

143

(for example, David, 1977; Journel and Huijbregts, 1978; Isaaks and Srivastava,

1989). The directions of the major and minor axes of the anisotropy are 010° and

280° respectively (Fig. 6.26).

In the major axis direction (010°), the variogram has a larger sill and a longer range

indicating a greater continuity. The more continuous ash distribution is probably a

result of the better correlation between clastic partings and ply ash content along this

direction. The larger sill (compared to the sample variance) is probably due to the

higher values of ash content along this direction, especially in the central and eastern

zones. In the minor axis direction (280°), the variogram has a smaller sill and a

shorter range indicating a smaller scale and lower degree of continuity. This

probably reflects the discontinuity of clastic partings in this direction. The sill does

not approach the sample variance and this may have resulted from the low values of

ash content along this direction.

6.4.3 Sulphur Content

The composite and ply sample sulphur data have similar statistical characteristics,

such as means (0.42% and 0.45%) and variances (0.07%2 and 0.09%2, Table. 6.1).

The histograms, probability graphs and skewness show similar populations (that is,

strong positively skewed distributions; Fig. 6.27). The two types of data have an

excellent correlation (Fig. 6.28). Because ply samples have higher proportions of

clay partings than composite samples, the similarity indicates that sulphur contents in

the coal portions are not significantly different to the sulphur contents in the partings.

This is also indicated by an independent relationship between ash content and sulphur

content in the coal samples. Therefore, using either data set in further statistical

144

analysis would also provide a similar result.

Compared to the thickness and ash content data, sulphur content is the most variable

parameter in the Sangatta seam (with coefficients of variation of 0.62 and 0.67,

Table. 6.1). However, in a spatial context, the sulphur content shows a high

regularity and continuity as indicated by the contour map, trend surface and

variogram analyses (Tables 6.2, 6.3).

The spatial distribution of sulphur content shows a clearer pattern compared to the

thickness and ash content data, as shown by the contour map (Fig. 6.29). The higher

regularity is confirmed by the higher correlation coefficient for the trend surface

analysis (Table 6.2). The first order trend surface map indicates an increase in the

sulphur content to the southwest from 0 to 0.8%, with a distinct negative residual in

the central zone (Fig. 6.30). The lowest value of the sulphur content in the central

zone (0.2%) is confirmed by the fourth order trend surface m a p (Fig. 6.31). A

similar pattern is also shown by the moving average m a p (Fig. 6.32), where the

sulphur content increases to the southwest (from 0.2% to 0.7%) and to the southeast

(from 0.2% to 0.5%).

The omnidirectional experimental variogram for the sulphur content data shows a

large range (1500 m ; Fig. 6.33). This is probably the effect of a strong spatial trend

with the slopes having the lowest angles oriented towards 100° (Fig. 6.34). The

directional variograms resulted in an anisotropy characterised by different slopes and

ranges (Fig. 6.34). This anisotropy is called slope and range anisotropy

(Zimmerman, 1993) or zonal anisotropy (Joumel and Huijbregts, 1978; Isaaks and

Srivastava, 1989). In the 100° direction, the variogram has the gentlest slope, the

145

largest range and smallest sill. In this direction the sulphur content changes

gradually with a low gradient and the data are correlated over a relatively long

distance. In the 010° direction, the variogram shows a steep slope indicating a rapid

change in sulphur content.

A different anisotropic feature is observed in the directional variograms for the

eastern area (Surya and Hatari Pits). Here, the major axis of the anisotropy (022°)

has a perfect trend, whereas in the minor axis direction (292°) the variogram is

erratic but has an extremely low sill.

The highest variability for the sulphur data may have resulted from a rapid change in

the values from across the coalfield. The higher spatial regularity and continuity,

however, indicate that the change has followed a pattern that was probably

significantly controlled by conditions in the peat depositional environment.

The rapid increase in the sulphur content to the southwest may have been influenced

by the increase in the sulphur content at the top of the Sangatta seam in this

direction (Chapter 4). This possibly corresponds to a general overall drowning of the

seam during the late stage of peat deposition, where the southwestern area subsided

more rapidly than the northeastern area. The highest degree of continuity (with a

good trend) towards 100° may indicate that this direction could have been the

inundation strike in the peat swamp.

Compared to the western area, a better trend for sulphur content was found in the

eastern area. This trend may have been caused by a greater subsidence relative to

the western area whereby in the eastern area, the southwestern part became inundated

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progressively by salt or brackish water.

6.4.4 Air Dried Moisture Content

The moisture data show a negatively skewed distribution (Fig. 6.35) with an average

value of 5.24%. The data vary from 4.00% to 7.10% with a range index of 0.59.

The standard deviation and variance are 0.63% and 0.40%2 respectively. The

coefficient of variation of 12% indicates a quite low variability for moisture content,

but if compared with other rank parameters (calorific value and volatile matter) the

moisture content is more variable. The low variation indicates that the rank of the

Sangatta seam is quite uniform. However, the higher variability for moisture content

than for other rank parameters suggests that the moisture content is probably also

influenced by other factors such as mineral matter.

The contour map for moisture content shows a decrease in the values eastward. This

decrease is more apparent on the moving average map (Fig. 6.36) and the trend

surface map (Fig. 6.37). A clear north-south trend for the average value is seen on

the moving average contour map, where the moisture content decreases slightly

eastward from 6.5% to 4.8%. The first order trend surface map indicates a

northeast-trending surface dipping toward the southeast. The surface is well fitted to

the moisture content with R = 0.66 and is significant at 99.99% confidence level.

The third order trend surface map has R = 0.74 and is significant at 99.99%

confidence level (Fig. 6.37b). It indicates a north-trending surface having a synform

in the central part, where the moisture content is lowest The low values in this part

are also indicated by negative values in the first order residual map.

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The omnidirectional variogram for moisture content shows a trend and a nugget effect

(Fig. 6.38a). The directional variograms indicate a slope anisotropy where the

gentlest slope and greatest nugget effect are observed in the direction of 020° (Fig.

6.38b). The greatest slope is observed towards 290°, where the moisture content

changes consistently with a relatively high rate.

The spatial variability of the moisture content may have been influenced by the

coalification processes occurring in the seam. The general decrease in the values

toward the east corresponds with increasing organic metamorphism. However, the

inversion encountered in the central part of the southern coalfield may indicate an

influence of depth of burial or folding (Lembak Syncline), where the moisture has

been reduced because of deeper burial and/or inherent water release from the most

fractured areas in the hinge zone.

6.4.5 Calorific Value and Volatile Matter.

One of the best rank parameters for coal below the rank of high volatile bituminous

is the calorific value calculated on a moist mineral matter free basis. In the ASTM

system, the value is given in British Thermal Units per pound (BTU/lb; Wood et al,

1983).

The calorific value data from the Sangatta seam are positively skewed (Fig. 6.39)

with the mean, standard deviation, variance and range index of 13520 BTU/lb, 187

BTU/lb, 34969 (BTU/lb)2 and 0.08 respectively. Among the coal parameters

analysed, the calorific value data have the lowest spread and a coefficient of

variation of only 1%. In general, the low variability in calorific value data may

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result from a uniform coalification. However, the pattern on the contour m a p

indicates an ordered gradual change of values across the area studied.

The contour map shows an increase in calorific values toward the southeast from

13250 to 13700 BTU/lb (Fig. 6.40a) with the increase more apparent on the moving

average (Fig. 6.40b) and trend surface maps (Fig. 6.43c). The first order trend

surface has a moderate correlation coefficient (R=0.58) and is significant at the

99.99% confidence level. It indicates a northeast-striking surface where the values

gradually increase toward the southeast.

However, the second order trend surface map (R=0.66 and significant at 99.99%

confidence level) indicates that in the central part of the coalfield, an inversion in the

rank occurs (Fig. 6.41b). This is also indicated by concentrations of negative

residuals in the central area as shown by both the first and second order trend

surfaces. The rank inversion in the central area is also indicated by the second order

trend surface m a p of moisture content and probably corresponds with the inversion of

the calorific value distribution. The possible causes of this rank increase and the

inversion are discussed in Chapter 5.

The omnidirectional variogram indicates that the distribution of the data followed a

trend although it shows a significant nugget effect (Fig. 6.42a). The directional

variograms show a slope anisotropy indicating different rates of change in various

directions (Fig. 6.42b). In the north-south direction, the variogram has a small sill

value indicating less variability. In the east-west direction, the variogram shows a

trend, but is erratic near the origin. The rate of change in the calorific values is

greatest in this direction. This is consistent with the trend surface m a p which

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indicates a gradual increase toward the southeast.

The volatile contents, which were computed on a dried ash free basis (daf), is a

good parameter for determining coal rank, especially for high rank coals (Stach et

al, 1982) and may also relate to initial conditions of sedimentation (Newman and

Newman, 1992). However, inconsistent coalification processes override the initial

volatile signatures of coals.

The volatile matter data are normally distributed (Fig. 6.43) with a mean, standard

deviation, variance and range index of 46.86%, 1.03%, 1.06%2 and 0.16 respectively

(Table 6.1). The coefficient of variation is quite low (0.02) and indicates low

variability for the volatile content

Generally, volatile matter in the Sangatta seam decreases eastward (Figs 6.44a,

6.45a). The lowest values however, are seen in the central-eastern part of the

southern coalfield (Figs 6.44b, 6.45b). Trend and anisotropy are indicated in

omnidirectional and directional variograms of the volatile matter data (Fig. 6.46). In

the Sangatta seam, the volatile content variations appear to be more related to

changes in the degree of coalification in the seam.

A corrected volatile content (by the corresponding calorific value) resulted in delta

values for volatile contents where the delta values are free from the influence of rank

(Newman, 1989) and, therefore, they probably indicate initial volatile matter

generation in the coal. A contour plot of the delta volatile content for the Sangatta

seam shows a low value in the east (Fig. 6.47) although this does not appear to be a

direct result of the liptinite content.

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The trend surface and variogram analyses indicate a similar pattern between the three

rank parameters of moisture content, calorific value and volatile matter. Although

these rank parameters are not well correlated, the statistical features suggest that they

are related spatially and this indicates an obvious pattern in the coalification.

6.4.6 Ash composition

Coal ash is derived from inorganic materials remaining after the coal is burnt It

consists of decomposed residues of silicates, carbonates, sulphides, other minerals and

organic constituents in the plant tissue. The chemical composition of ash may

provide useful information about the minerals present in the coal (Ward, 1984).

The coal ash from the Sangatta coal samples is mostly composed of Si02, A1203,

Fe203, Ti02, CaO, M g O , N a A K 2 0 , P205, M n 3 0 4 and S 0 3 (Appendix 6.5). The

oxides are grouped according to their occurrence, as indicated by the R-mode cluster

analysis (Fig. 6.48). This may correspond to the source minerals. Si02, A1203, K 2 0

and Ti02 may have been derived from clay and silicate minerals whereas the rest of

the oxides may have been formed during the decomposition of carbonates, sulphides,

sulphates and phosphates.

The distribution of the clay and silicate minerals tends to increase slightly toward the

southeast (Fig. 6.49a). Higher values in the western and eastern areas are indicated

by the moving average (Fig. 6.49b), first order residual and second order trend

surface maps (Figs 6.50a, 6.50b). The distribution pattern for the oxides of this

group may be related to the presence of clay partings in the seam, which are only

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well developed in the upper part of the seam in the central area. This is confirmed

by an increase in the silica to alumina ratio (SiO^M203) toward this area (Fig. 6.51)

and probably corresponds to the smaller proportion of clay minerals in the inorganic

matter. This may also correspond to the higher proportion of the carbonate, sulphide

and sulphate derived components (second group) in the central part.

The carbonate-, sulphide- and sulphate-derived oxides tend to decrease toward the

southeast (Fig. 6.52a). The higher values in the central area are shown by the

moving average (Fig. 6.52b), first order residual and second order trend surface

maps. The higher concentration of the oxides in this group may be related to the

concentration of syngenetic carbonate in the central area and this was probably

controlled by higher water levels during the later stages of peat deposition (Chapter

5). This is further supported by an increase in MgO and CaO+MgO contents in the

central area (Figs 6.53, 6.54).

Having assumed that most C02 has been derived from carbonate minerals, a positive

correlation between ash content and C02 implies a significant contribution of

carbonate to the-ash. The high correlation between C02 and CaO and MgO suggests

that these are mainly derived from dolomite. The dolomitic and sideritic nodules

observed in some coal samples from the central area indicate a syngenetic origin and

may have been formed during early diagenesis under slightly oxidising conditions

(Ward, 1984; Spears, 1987). Gluskoter et al. (1981) and Spears (1987) pointed out

that sideritic nodules, in particular, are commonly formed in fresh water conditions

where sulphate species are low.

Alternatively, the distribution of the carbonate-derived oxides may have been

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controlled by the intensity of cleats in the seam, for example in the central area

(hinge zone of the Lembak Syncline) jointing is probably relatively intense. Coal

petrographic data indicates that the carbonate is epigenetic in many coal samples

(mostly as fracture infilling), thus supporting this interpretation.

6.4.7 Ultimate Analysis Data

Coal macerals are normally composed of the chemical elements carbon, hydrogen,

oxygen, sulphur and nitrogen, hereafter termed the organic elements. Ultimate

analysis determines the percentage of these elements (see Appendix 6.6).

The Sangatta coal contains carbon, hydrogen and nitrogen respectively ranging from

71.6% to 82.3% (average 79.5%), 4.5% to 5.9% (average 5.5%) and 1.2% to 2.1%

(average 1.6%). In the Sangatta seam, with the exception of nitrogen, the organic

elements show a random distribution without any significant pattern. This is

probably because the predictable pattern has been obscured by several factors such as

the occurrence of the inorganic elements (for example, most of the organic elements

are also found in the associated inorganic matter, for example, Ward, 1984) and the

coalification process (for example, hydrogen would be reduced during coalification).

Therefore, for the Sangatta seam, it may be inappropriate to explain the lateral

variations of organic elements in a palaeoenvironmental context.

Among the ultimate analytical data, nitrogen tends to increase toward the east (Fig.

6.55). Because nitrogen is commonly associated only with organic matter (Ward,

1984), the lateral variations can be explained in the context of the environmental

conditions in the peat swamp. The high nitrogen content may be related to an

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extensive microbial reworking of the peat-forming vegetation (Diessel, 1992). In the

central area, this is probably related to the higher water level during the last stage of

peat accumulation which increased the pH value. In this area, it may also

correspond to the high content of detrovitrinite (Chapter 5) as this maceral indicates

a higher degree of decomposition (Bustin and Lowe, 1987; Andriesse, 1988).

6.4.8 Types of Sulphur

In coals, sulphur is commonly present in organic and inorganic forms. The organic

sulphur normally occurs in organic compounds and its occurrence is controlled by the

types of plants and the hydrologic conditions in the peat swamp. The inorganic

sulphur is most commonly present as pyrite which occurs as either syngenetic or

epigenetic forms.

In the Sangatta seam, the principal sulphur is organic sulphur as indicated by the

high ratio of organic to inorganic sulphur and the high positive correlation between

the total and organic sulphur (Fig. 6.56). The ratio varies from 1 to 10 and tends to

be highest in the western, southern and eastern areas (Fig. 6.57). This may indicate

that, in these areas, the transformation of organic sulphur to pyrite (inorganic

sulphur) was less extensive under the influence of brackish water.

However, in the uppermost parts of some sections of the seam, where the total

sulphur content is significantly elevated (Chapter 4), the principal sulphur is probably

present as pyrite. This is consistent with the observations of framboidal pyrite in

some coal samples from the top of the Sangatta seam in the central area. Because

the pyrite-rich zones are commonly very thin, the effects are not apparent in the

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composite sulphur content

6.4.9 Multivariate Features of Coal Data

A product moment correlation coefficient matrix measured by the cluster analysis

program (Jones and Facer, 1982) indicates that, in general, most of the major coal

parameters (thickness, ash content and sulphur content) for the Sangatta seam are not

correlated to each other. However, if the coalfield is divided into areas, the

correlatability of parameters in specific areas is significantly higher.

In the central area, there is a negative correlation between composite ash content and

composite and ply sulphur contents. However, ply ash content and ply sulphur

content indicate a positive correlation. The negative correlation suggests that the

sulphur content was probably more related to the organic constituents rather than the

inorganic constituents. However, the positive correlation between ply ash content and

ply sulphur content may indicate that in the central area, the sulphur content in the

partings is slightly higher than in the coal. The correlation between thickness and

ply sulphur content is probably the effect of elevated sulphur at the top of the seam,

especially in the thicker parts, due to a relatively rapid subsidence.

In the western area, the correlation between ply and composite ash contents is

significantly higher. The positive correlation indicates the important control of thin

partings on composite ash content because the thin partings are also included in the

composite samples but not in the ply samples. A negative correlation between

composite ash content and composite sulphur content again suggests that the sulphur

is probably not controlled by the presence of inorganic matter, but by the organic

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materials.

In the eastern area, a very weak correlation, but the best for all areas, is between

thickness and ply ash content. This may be connected with a disturbance in seam

development by clastic interventions; where partings are well developed, the

development of coal was retarded.

6.5 SUMMARY

Statistical analysis has been used to extract meaningful and interpretative information

from the imperfect and large set of thickness and chemical data from the Sangatta

seam. The benefits of this analysis include:

1. amplification of the general structure of the data using basic

(descriptive) statistics;

2. better classification of the data using cluster analysis;

3. delineation of the spatial trends in the data using trend surface analysis

and- moving window statistics; and

4. measurement of the spatial continuity and variability (spatial structure)

of the data using variogram analysis and moving window statistical

analysis.

Such information is extremely useful for geological interpretations and reserve

estimations in that they improve the confidence level in the coal resource assessment.

Histograms and probability graphs, supplemented with the basic descriptive statistics

156

(for example, mean and standard deviation), allowed recognition of the different

characteristics between coal parameters (for example, thickness, ash content and

sulphur content). This basic statistical tool also elucidated the differences in the

characteristics of specific coal parameters between different areas (for example, a

significant difference in the thicknesses in the E-West and Hatari areas). These

differences should be influenced by the geological conditions in the areas.

Trend surface and moving window analyses allowed interpretation of the directions of

change in several coal parameters (for example, thickness, ash content and sulphur

content). When deciding orders (or degrees) of trend surfaces that should be used in

geological interpretations, the geological knowledge of the area should also be

considered. The coefficients of correlation from trend surface analysis are also

considered to be significant in determining the degree of regularity in the spatial

distributions of each coal parameter.

Variogram and moving window analyses permitted determination of the spatial

continuity and variability of coal parameters and characterised the changes in the

variabilities from one area to another. Some coal parameters provided well-defined

variograms whereas others gave obscure features. The variograms presented the

spatial continuity and variability of each coal parameter in a quantitative manner.

Trends were also shown by the variograms. For specific parameter variograms, it

was possible to recognise isotropy or anisotropy in the distributions, that is, it was

possible to recognise different spatial characteristics in various directions.

Multivariate correlations were not a significant part of this study and was only used

where the data was selected according to a specific area (or block). Interestingly

spatial relations between some coal parameters are significant, although most of the

157

parameters could not be correlated statistically.

An important feature of the geostatistical analysis undertaken in this study has been

the recognition of the variations of statistical characteristics between coal parameters

and within parameters for the different areas (for example, Figs 6.58, 5.59). It is

believed that the differences reflect the specific geological controls and settings that

were active in each area during the formation of the coal.

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159

CHAPTER SEVEN

DEPOSITIONAL ENVIRONMENT OF THE SANGATTA SEAM

7.1 INTRODUCTION

Peat accumulation is generally controlled by two major factors - allogenic (tectonic)

and autogenic (environmental) factors (McCabe and Parrish, 1992; Flores, 1993).

Allogenic factors include climate, tectonism and eustacy, and control the number,

thickness, continuity and chemistry of seams, on a large scale, for example, on a

basin-wide scale (McCabe, 1991; Galloway and Hobday, 1983). Autogenic factors

including vegetation types and hydrologic conditions control the geometry and quality

distribution in seams on a local scale (peat swamp scale).

In this chapter, the data gathered in previous chapters is integrated into models for

the depositional environments of the Sangatta seam. Firstly, these models are

discussed in the context of a broader scale of sedimentary and tectonic development

of the Sangatta Coalfield in the northern Kutei Basin. Detailed depositional models

of the Sangatta seam were formulated mainly on the basis of the information from

sedimentology, seam geometry, coal petrology and statistical parameters of thickness

and quality data.

7.2 TECTONIC AND SEDIMENTARY CHARACTERISTICS OF THE KUTEI

BASIN

The Kutei Basin is one of the Indonesian basins which has a high tectonic mobility,

160

but the tectonic development has not been well understood. In general terms, the

basin is characterised by thick sedimentary strata indicating complex lateral and

vertical relationships. Many lithostratigraphic units in the Kutei Basin change quite

rapidly laterally from fluviatile in the west to marine environments in the east. In

some places such facies changes occur over a distance less than 10 k m (for example,

Nas and Indratno, 1979; Land and Jones, 1987; Muggeridge, 1987). The presence of

numerous seams (in places more than 50 seams, for example, Land and Jones, 1987)

is probably another indicator of the tectonic instability in the Kutei Basin (see

Diessel, 1992).

However, the tectonic and sedimentary characteristics vary across the basin according

to the palaeogeographic positions in the basin. These variations have resulted in

different features in the sedimentology and coal geology of the basin. In general, the

Mahakam area, which is located in the central region of the Kutei Basin, has thicker

Tertiary strata than any other area in the basin. A comparison of the Sangatta area

(located near the northern margin of the Kutei Basin) and the Mahakam area show

differences as recorded below.

1. Tertiary sediments are thicker in the Mahakam area.

2. Syn-sedimentary deformational structures, such as slump structures, are

more extensive in the Mahakam area.

3. There are more seams occur per unit sedimentary thickness in the

Mahakam area.

4. In general, the seams are thinner in the Mahakam area.

5. The seams are relatively widespread in the Mahakam area, as inferred

from an 800 m suggested drill spacing for measured reserve calculations

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(Land and Jones, 1987).

6. Mahakam coals have a relatively high ash yield.

These differences were probably caused by several geological factors such as:

1. Clastic sedimentation in the Sangatta area was not as extensive as in the

Mahakam area and this was probably controlled more by limited

subsidence and lack of sedimentation space.

2. The Sangatta area was located near the margin of the basin where

subsidence was not as rapid as in the Mahakam area. The thicker

seams in the Sangatta area indicate a better balance between subsidence

and peat accumulation over a long period of time (McCabe, 1991).

3. In the Sangatta area, rivers were probably not as large as in the

Mahakam area.

The effect of such tectonic and sedimentary features on sedimentological and coal

geological aspects in the Sangatta area are discussed in the following section.

7.3 SEAM DEVELOPMENT

The nature of the northern Kutei Basin (the Sangatta area) has resulted in different

sedimentary features compared to the central part of the basin. This was probably

caused by sedimentation taking place in a different system independent of the main

system in the Mahakam area.

In the Sangatta Coalfield sedimentation took place in a depositional setting which

162

was located close to a source area along the northern margin of the basin. Rapid

lateral changes in the sedimentary facies from fluviatile in the northwest to marine

environments in the southeast were c o m m o n in this setting. This m a y imply a

greater depositional gradient compared with the central part of the Kutei Basin.

The sedimentary development is characterised by a general regressive trend from the

Pemaluan through Pulubalang to Balikpapan Formations. This regressive trend from

more marine to more fluvial depositional environments is indicated by the

sedimentological associations and is also reflected by the seam development in this

area. However, in the Balikpapan Formation sedimentological data indicate an

upward decrease in stream energy probably caused by an increase in the basin

maturity or by a rise of sea level.

In the Sangatta area, more than twenty seams have been deposited within a package

of fluvio-deltaic sedimentary rocks (Fig. 2.8). The seams reflect a change from a

more marine influence in the Pulubalang Formation, indicated by a higher sulphur

contents and thinner coals, to fresh water and thicker coals in the Balikpapan

Formation. The most prolific coal-bearing strata are in the Balikpapan Formation,

which was mostly deposited in fluvial dominated environments.

The six main seams, namely the Prima, Bintang, Sangatta, Middle, Pinang and

Kedapat seams respectively from the bottom to the top of the sequence, indicate a

general westward shift of the depositional centre. However, fluctuations in the base

level during the deposition of the seams was caused by sea level changes and

subsidence.

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7.4 DEPOSITIONAL PARAMETERS OF THE SANGATTA SEAM

In terms of geological and economical points of view, the Sangatta seam is the most

important seam in the Sangatta Coalfield. This seam has been explored intensively

and is currently the basis of the coal production in the Sangatta Coalfield.

7.4.1 Clastic interseam strata

Although the sedimentary platform of fluvial strata, on which the Sangatta seam was

deposited, cannot be determined in detail on the basis of the data available for this

study, the characteristics of fluvial channels and the overbank sediments associated

with the seam were recorded. These characteristics may be related to the distribution

pattern and physical and chemical properties of the seam.

1. Coarse-grained sedimentary strata deposited in fluvial channels and crevasse

splay areas were found in several locations. They record different channel and

crevasse systems which occurred below, above or contemporaneously with the

Sangatta seam. -Several channel and crevasse sandstone bodies that are related to the

Sangatta peat deposition are:

(i) Channel A sandstone body. This channel was active before the

deposition of the Sangatta seam. Evidence for the presence of this

channel was gathered from geophysical logs in the E-West area (C3486

and C2982). At this location, the sand body appears as an interburden

between the B2 and Sangatta seams and is approximately 15 m thick.

A southeast flow direction was interpreted on the basis of the locations

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at which the sand body was recorded. This channel also influenced the

clastic sedimentation at the bottom of the Sangatta seam in the western

zone (see Chapter 4).

(ii) Channel B. This channel is not recorded in the available data, but the

extent of the channel can be interpreted from crevasse splay and

overbank deposits found in the Sangatta seam (E-West). This channel

probably flowed in a southeasterly direction in the western part of the

Sangatta Coalfield.

(iii) Channel C sandstone body. This channel probably had an easterly trend

through the central part of the Sangatta Coalfield (approximately 19600

to 19700 northing coordinate, Fig. 7.1).

Several features recorded relating to this channel (Channel C) are:

(i) an extensive sandstone outcrop in the northern part of Hatari Pit (Fig.

7.1, point 1) where the Sangatta seam is absent and appears to have

been eroded by the channel; palaeocurrent measurements at this location

indicate that this channel had a southeasterly flow direction.

(ii) the absence of only the Sangatta seam along the channelised zone (Fig.

7.1, point 2) suggests that the channel was active mostly during the

period of the Sangatta peat deposition; the sedimentological profile (MS-

8 in Fig. 3.16) indicates that this channel may have been stacked mostly

in the same position before and during the peat accumulation, although

several times it formed crevasse splay and crevasse channel deposits to

the south along the top surface of the Sangatta seam (Fig. 7.3, Channel

D).

165

(iii) the increase in the ply ash yield towards the channel may have resulted

from a clastic influx from the channel.

(iv) the channel zone may have controlled compactability of the sedimentary

rocks beneath the Sangatta seam because in the early stage the channel

was probably wider; the subsequent development of the channel seemed

to be similar to the model reported by Stanistreet et al (1993; Fig. 7.2)

where vegetation and peat deposit occupied part of the initial channel

sand and confined the subsequent channel in a narrower belt; along the

initial channel the sediments were less compactable whereas in areas

distal from the channel the sediments were more compactable.

2. Fine-grained sediments occur as either massive or laminated silty mudstone units

closely related to the Sangatta seam. The massive silty mudstone occasionally has

the features of an underclay (sometimes rooted) and may have developed as soil

horizons where the Sangatta peat vegetation initially grew. The silty mudstone is

pale if developed as floodplain deposits and darker when developed as swampy

floodplain deposits. The laminated fine-grained sediments mainly found as the clastic

roof of the Sangatta seam were deposited either in a swampy floodplain or lacustrine

environment when the peat surface subsided below the regional base level. Thin

units of laminated fine-grained sediment were also found in the floor of the seam at

some localities. These laminations are the products of intercalations of sediments of

different size and colour, including mud-silt or shale-coal intercalations. Fine

grained sediments, especially laminated shales, are also found as partings within the

Sangatta seam. The nature of the partings indicates water transported materials,

probably deposited by the major alluvial channel systems in this area.

166

From the above information, a model was erected for the depositional environments

of clastic sediment closely associated with the Sangatta seam (Fig. 7.3). Although

the model is not to scale, it indicates that the peat swamp of the Sangatta seam was

located quite close to the rivers. The lithological character of the clastic strata below

and adjacent to the seam are believed to be an important factor governing the initial

distribution of the Sangatta peat. In addition, this association may have controlled

the occurrence of subsequent processes, such as faulting and erosion, in the peat

body.

7.4.2 The Sangatta Seam

The Sangatta seam was deposited on a floodplain of the ancient Sangatta fluvial

system. The variations in coal thickness and quality characteristics indicate that the

seam may have been deposited in a peat swamp whose morphology and water

conditions varied on a quite local scale. The thicker parts of the seam are more

uniform than the thin parts where the thickness becomes more variable. O n the basis

of the sedimentology and coal geology, the Sangatta peat can be categorised into 4

zones namely western, central, eastern and northern zones (Figs 7.1). The

characteristics of the Sangatta seam in each zone are summarised in Figures 7.4 and

7.5.

Western Zone

In this zone the Sangatta seam is commonly underlain by a massive bioturbated pale

silty mudstone (seat earth with root traces). In some places, the mudstone is quite

thin and the seam directly overlies channel sandstone bodies which provided less

167

compactable material beneath the seam. The Sangatta seam is thickest in this

western zone. Away from the centre of this zone, where the seam is thickest, the

seam splits into several benches commonly separated by overbank sediments.

In the early stage, the Sangatta peat may have been deposited in a low lying fresh

water environment, indicated by a low sulphur content in the lower part of the seam.

High ash contents and the presence of shale partings in the lower part of the seam

suggest that the swamp was frequently influenced by muddy flood waters probably

from channels north and west of the peat swamp. Toward the middle part of the

seam, ash yield decreases dramatically and partings are absent. However along the

western margin of the western zone, high ash contents and numerous partings are

present. Sulphur content is consistently low from the bottom to the middle of the

seam. High sulphur is only recorded in the uppermost part of the seam as a

leaching effect from the high sulphur content in the overlying seam (Middle seam).

The whole seam is characterised by several distinctive features such as low nitrogen

content, low SiO/Al^ ratio and low Ca-Mg content.

Petrologically, the coal in the western zone is characterised by high telovitrinite,

telinite and vitrinite derived from angiosperm wood and correspondingly low

detrovitrinite and vitrinite derived from cork tissue. Vitrinite reflectance is lowest

and the variability of the reflectance within samples is highest in this western zone.

The statistical analysis of the Sangatta seam in the western zone indicates:

(i) a unimodal normal distribution for the thickness data, probably

indicating regular depositional conditions for the coal;

168

(ii) a relatively high regularity of the thickness data (indicated by a higher

correlation coefficient (R) and significance (F) from trend surface

analysis);

(iii) a high spatial continuity of the thickness data (indicated by the high

range of the variogram);

(iv) a high degree of isotropy of the thickness data (indicated by the

directional variograms);

(v) a low variability of the thickness data (indicated by the low coefficient

of variation obtained from moving window statistics and the low

nugget/sill ratio of the variogram); and

(vi) a low variability of the ash and sulphur data (obtained from the moving

windows statistics).

Centra] Zone

The north-south split between the Sangatta and Middle seams, probably caused by a

growth fault in the southern part of the Sangatta Coalfield, is the border between the

western and central zones.

The central zone occupies part of the Lembak Syncline hinge zone but is this area,

the elevation of the hinge zone is lower than expected, indicating that it had subsided

before folding (Chapter 4).

In the central zone, the clastic interseam strata between the Sangatta and Middle

seams are thickest. The sedimentology of this interval is characterised mainly by

overbank sediments. Sand bodies recorded in this interval are interpreted as crevasse

169

splay or crevasse channel and distributary channel deposits. The distributary

channels eroded parts of the Sangatta seam.

In this zone, the Sangatta seam, is underlain mainly by fine-grained strata although in

some drill holes, coarse-grained sediments are also recorded but they are relatively

thin and are interpreted as crevasse deposits (splay or channel). The seam is

relatively thin and washout zones occur at the top of the seam and small faults are

recorded. Clay partings are only developed in the uppermost part of the seam in the

eastern part of this zone.

The composite sulphur content is lowest in the central zone and increases towards

the southwest. This increase was caused mostly by an increase in sulphur content at

the top of the seam. Ash data from ply samples decreases towards the south. The

composite nitrogen and CaMg contents and SiO/A^ ratio are highest in the central

zone.

Petrographically, the coal is characterised by the highest detrovitrinite content and

cork/wood ration correspondingly it has the lowest telovitrinite and telinite derived

from angiosperm wood. The rank of the coal is the highest for the basin and the

variability of the vitrinite reflectance in each sample is low.

From a statistical viewpoint, in the central zone, the Sangatta seam is characterised

by:

(i) a bimodal thickness distribution;

(ii) a low thickness regularity;

(iii) a low spatial continuity (indicated by the low range value);

170

(iv) a high spatial variability (indicated by high coefficients of variation for

the moving window statistics and the high nugget/sill ratio of the

variogram);

(v) a strong anisotropy for the thickness spatial distribution; and

(vi) a high spatial variability for the ash data;

Eastern Zone

In this zone, the Sangatta seam is underlain by a thick unit of levee deposits with a

channel sandstone body recorded below these levee deposits. The latter was

probably the extension of the main channel that is so prominent in the northern part

of the eastern zone. The Sangatta-Middle seam clastic interval consists mainly of

fine-grained overbank sediments and small-scale channel sand bodies. Washouts

(some filled with sand and some filled with silts) are c o m m o n at the top of the

seam. Normal faults (some probably growth faults) are also common. Clay partings

are numerous and they vary in thickness over a short distance. T o the east, seam

thickness decreases and the seam splits into multiple seams where the intensity and

thickness of partings increases rapidly.

The seam is characterised by the highest ply ash contents, a low sulphur content, a

moderate nitrogen content, a high Si02/Al203 ratio and a low C a M g content. The

sulphur contents are consistently low from the roof to the floor of the seam.

Petrographically, the coal in this zone has moderate telovitrinite and detrovitrinite

contents.

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Statistically, the seam is characterised by:

(i) a bimodal thickness distribution;

(ii) a low thickness regularity;

(iii) a low thickness spatial continuity;

(iv) anisotropy of the thickness spatial distribution;

(v) a high variability of the thickness (indicated by a low coefficient of

variation obtained from the moving window statistics and low nugget/sill

ratio of the variogram); and

(vi) a high variability of both the ash yield and sulphur content (obtained

from moving windows statistics).

Northern Zone

In this zone, the Sangatta seam is underlain by overbank deposits that are commonly

associated with fluvial channel deposits in which the proportion of sandstone is

relatively high. The clastic interval between the Sangatta and Middle seams consists

of channel and overbank deposits. Washout zones are found at the top of the seam

and the intensity of partings increases towards both the north and south. Some faults

(probably growth faults) occur.

From the centre of the northern zone, the ash content increases both to the north and

south. Sulphur content is low and it is consistently low from the top to the bottom

of the seam.

Petrographically, the coal has high telovitrinite and telinite derived from angiosperm

wood contents; the cork/wood ratio is low.

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Statistically, the Sangatta seam is characterised by:

(i) a unimodal thickness distribution;

(ii) a high thickness regularity;

(iii) a high spatial thickness continuity;

(iv) a high degree of isotropy; and

(v) a low thickness spatial variability.

7.5 DEPOSITIONAL HISTORY OF THE SANGATTA SEAM

Some of diagnostic factors used to interpret the general depositional setting of the

Sangatta seam are the fluviatile sedimentary association, the low ash and sulphur

contents, the high vitrinite and low inertinite contents and the amount of organic

matter derived from trees.

Several general models could be formulated to interpret the depositional history of

the Sangatta seam in the Sangatta Coalfield.

Possible explanations for the low ash and sulphur contents of peat that is located on

a fluvial-deltaic floodplain are - elevated (raised) peat swamps, floating peat swamp,

filtering and confinement of the peat by channels; chemical leaching of minerals

from the peat and sedimentary bypassing.

Elevation of the peat forms a raised bog and the peat swamp is protected from

clastic detritus and sea water incursions.

173

A floating organic mat also protects the peat swamp from clastic influxes. However,

a floating swamp is not a suitable model for the clean Sangatta coal because when

the peat is eventually deposited on the floor of the lake or body of water, it would

be associated with clastic sediments (Moore, 1989). Additionally, floating swamps

are typically composed of non-woody vegetation (Moore, 1989) and this contrasts

with the Sangatta peat which contains significant woody tissue. If a floating peat

mat was the precursor, vegetation would have accumulated only during the earliest

stage of the peat development (Diessel, 1992).

Filtering by a dense vegetation screen would protect the central part of a peat swamp

away from clastic influxes. However, this would need an extremely dense vegetation

and a relatively wide vegetation screen to protect the peat swamp from all clastic

sedimentation. This might not have been the case for the Sangatta peat, because the

swamp was juxtaposed against fluvial channels.

Dense vegetation and peat accumulation also controls the pattern of clastic

sedimentation (McCabe, 1984; McCabe and Shanley, 1992; Stanistreet et al, 1993).

In fluvial systems, levee and floodplain vegetation and peat deposits confine clastic

sedimentation to channel belts. Stanistreet et al. (1993) reported that clean peat

occupies the wide levee area of the meandering Okavango river in Bostwana,

southern Africa. The clean character of the peat results from a lack of clastic

incursions into the peat swamp. This happens because the amount of fine-grained

sediments suspended in the river water is almost nil, even during flooding events

(due to minimum supply of fine-grained sediments from the catchment area).

Moreover, confinement of the river channel by the dense vegetation and peat layer

results in minimal crevasse clastic discharge to the peat swamp.

174

The levee vegetation and peat of the Okavango river are frequently subject to

burning because of the seasonal dry climate. The fires have destroyed the vegetation

and peat to produce incompletely-burnt organic fragments called 'burnt ash' by the

authors. The problems of burning, together with the lack of fine-grained sediments

required for the peat to become buried (preserved), suggest that the Okavango peat

would never become an economic seam. However, Caincross et al. (1988) used

these fluvial deposits as modern analogues for the Permian Witbank coal (South

Africa). While the Okavango model cannot be used in its entirety for the generation

of the Sangatta seam, some aspects of the Okavango system, such as channel

confinement, are comparable with the ancient channel development in the Sangatta

area (see Section 7.4.1).

Mineral contents in peat would decrease significantly as a result of dissolution of

soluble mineral components and their subsequent expulsion from the peat by

compactional water (Diessel, 1992). The role of chemical leaching in the reduction

of ash in coal was suggested by Kosters et al. (1987). From their experiment, they

concluded that leaching decreases ash by 1/5 to 1/3 and this reduction also occurs

during early digenesis of peat. However, McCabe and Breyer (1989) doubted the

influence of leaching because information on leaching of buried peat was not

available in Kosters' et al. (1987) report.

Staub and Esterle (1993) attributed the accumulation of clean, low ash peat deposits

on the Sarawak lowlands was attributed to sedimentary bypassing on the delta

front/coastal plain. These authors suggested that sediment load in the rivers was

dominated by suspended materials which were transported directly to the river mouth

175

mostly within the lower layers of the stream water. This caused a minimal amount

of inorganic material to enter the peat swamp during flooding. The stratification of

the sediment load was mainly caused by acid water accumulating preferentially in the

upper layers of the streams by percolation and discharge of surface water from the

adjacent peat bodies during high rainfall. However, the sedimentological features in

the Sarawak lowland setting are not entirely comparable to the interseam strata of the

Sangatta seam, because many channels in the latter are composed of sandstone units

which are occasionally associated with crevasse splay deposits. Furthermore, beach

sands, which commonly underlie the peat deposits on the Sarawak lowlands, are not

recognised in the Sangatta coal association.

From the above discussion, and from the zonation of the seam properties, it is

suggested that the Sangatta seam was probably deposited in a raised bog environment

on a fluvial floodplain. The extremely high vitrinite content suggests that the bog

was vegetated by woody plants and the bog wetness was maintained by a high

rainfall. The low ash in the seam may have been a result of confinement, over a

period of time, of river channels and by the thick and dense Sangatta peat and

vegetation. The high rainfall may have also retarded oxidation processes on the peat

surface as indicated by the low inertinite content (Cohen et al, 1989; Esterle and

Ferm, 1990). The raised bog was juxtaposed against contemporaneous alluvial

channel systems. Examples of extensive peat accumulation and clastic deposition

have been reported from modern and ancient geological records (for example,

Anderson, 1964; Moore, 1991; Staub and Esterle, 1993).

Although many tropical raised peat swamps have developed from a low moor peat

with brackish water influence into a raised bog (for example, Anderson, 1964, 1983;

176

Esterle et al, 1989; Esterle and Ferm, 1993), such development did not occur in the

Sangatta peat swamp. Chemical and petrological data suggest that most of the peat

accumulated in fresh water conditions.

Whereas the above discusses general aspects of the Sangatta peat development, a

more detailed model for the Sangatta peat swamp has to be developed on the basis

of distinctive vertical and lateral variations in the sedimentology of associated rocks

and in the geochemical, petrological and statistical parameters within the seam. The

causes of zonation in thickness, maceral compositions and some chemical parameters

are examined in connection with the peat depositional conditions. Thus, the

geological processes that took place in each zone are discussed based on the basis of

information from section 7.4.2.

Model 1 (Fig. 7.6a)

In this model the western zone has been interpreted as the highest part of a peat

swamp (raised bog). This part of the peat swamp was laid down on the Channel A

sand body. The extremely low inorganic content of the coal (especially in the centre

of this zone) indicates that this zone was almost never touched by clastic deposition.

The thickness and continuity of the seam suggest a high rate of peat accumulation

that kept pace with the rate of subsidence. The peat swamp was occupied

dominantly by woody vegetation as indicated by the high content of macerals derived

from angiosperm wood. Because of the high acidity in the swamp water resulting

from decomposed organic materials (humic acid), bacterial activity was retarded and

this slowed degradation of the vegetal matte, High preservation of plant tissues is

indicated by the high proportion of telinite in this zone. The more uniform (less

177

spatially variable) thickness and the absence of channelling effects in the western

zone indicate that subsidence mainly resulted from self compaction of the thick peat.

The central and eastern zones are interpreted as low-moor areas. The decreased

thicknesses indicate a low peat productivity and a higher rate of decomposition. The

high detrovitrinite and nitrogen contents (especially in the central zone) indicate that

the vegetation was dominated by herbaceous plants under high water conditions

where bacterial activity was also high (see Anderson, 1983; Titheridge, 1988; Moore,

1989). Clastic input was more common in this central zone, especially in the upper

portion of the peat column. In the eastern zone, however, clastic deposition was

periodic, resulting in numerous partings and high mineral content in the peat; this

increased the preservation level of organic matter (Rimmer and Davis, 1988; Moore,

1989).

The low-lying character of the peat swamp in the central zone was probably the

result of faster subsidence. The subsidence took place continuously up to the last

stage of peat accumulation and, together with self-compaction of the peat body, this

zone (especially the central zone) became especially low. This allowed clastic

sediments to be deposited (including some channels). The high variability of the

peat thickness may have resulted from this geological process. In this zone, the peat

was thinner due to the low plant productivity, retardation of peat accumulation by

clastic domination and erosion of upper part of the peat.

The clastic sediments were deposited in the central zone as the peat and fine clastic

substrate subsided due to the load of overlying sediment; whereas in the western

counterpart, peat accumulation was still continuing. This caused the major eastward

178

splitting giving rise to the Sangatta and Middle seams. Once the central zone was

restabilised, the Middle peat began to accumulate.

Model 2 (Fig. 7.6b)

In this model the western and eastern zones are interpreted as the margins of a

raised bog whose centre was located in the central zone. Peat accumulation

commenced in a low-lying swamp, as indicated by extensive clastic partings at the

bottom of the seam. In the centre of the bog (in the central zone) the peat

accumulated at a relatively high rate. This resulted in a raised bog whose centre

was occupied by a mixed herbaceous (with high nitrogen content) and arborescent

vegetation (see Anderson, 1983). The high rate of decomposition as indicated by the

high proportion of detrovitrinite may have been the result of the low preservation

rates for herbaceous plants (Moore, 1989; Diessel, 1992). Because of the herbaceous

vegetation and the low bulk density (Anderson, 1983) the centre of the bog subsided

more rapidly due to self-compaction. The subsidence was accelerated by differential

compaction in the fine clastic sediments below the peat swamp (the central zone

sediment was more compactable). O n the margins of the raised bog, water was

deeper resulting in a high nutrient supply,, and consequently, a luxuriant woody

vegetation indicated by the high proportion of telinite in the coal. Parting

development at the edge of the western and eastern zones indicates contemporaneous

clastic activities and a short distance to the active river channels.

Model 3

peat swamp is interpreted as a low-lying

179

in some coal quality parameters is interpreted as the result of filtering effects from

very dense vegetation next to the river channels. Because the water table must have

been uniform over the swamp, zonation in petrological composition is more difficult

to explain in terms of the peat swamp conditions.

Appropriateness of the models.

The three models are compared in terms of the ability of each model to provide

adequate geological explanations for the geological features observed for each area of

the Sangatta seam.

As mentioned in Model 3, it is difficult to explain the areal zonation in petrological

composition of the Sangatta coal if the peat swamp was a low, flat moor. Moreover,

it is also difficult to believe the effectiveness of dense vegetation in filtering clastic

sediments from the peat swamp (over a sort distance) if the water table is uniform.

In this situation, where the swamp was contemporaneous with clastic activities, the

resultant peat should have been very dirty (McCabe, 1984, 1987). Therefore, the use

of this model to- provide an appropriate explanation becomes less plausible.

Model 1 provides an explanation for most of the geological phenomena in the seam.

However, the centres of raised bogs are usually occupied by more stunted vegetation,

which is commonly herbaceous as documented by authors such as Anderson (1964,

1983), Anderson and Muller (1975) and Moore (1989). This is not consistent with

the woody plant domination and low nitrogen content in the highest level of the

western zone of the Sangatta seam, because in model 1, this zone is interpreted as

the centre of the raised bog.

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Thus shortcomings of Model 1 are overcome with Model 2 where more geological

variations between zones can be accommodated. However, some of the geological

parameters need to be further explained, for example, the high carbonate content,

high cork tissue content, high S i O / A l A ratio, high sulphur content at the top of the

seam and the presence of framboidal pyrite at the top of the seam in the cental zone.

While more detailed work is still needed, several explanations can be attempted to

explain the reasons for the peculiarities of some seam characteristics. The high

content of cork tissues in the central zone necessitates an increased cork/wood ratio

in the herbaceous peat vegetation. The high S i O / A l A ratio was probably the result

of a decrease in clay content in the inorganic component since the central zone has

been interpreted as the centre of a raised bog and above the regional water table.

The high sulphur content and the presence of framboidal pyrite at the top of the

Sangatta seam in southern part of the central zone suggest that, at the last stage in

the peat development, this area was inundated by brackish or marine water.

Comparison between the Sangatta and Bukit Asam Al seams.

Another important exploited Miocene Indonesian coal deposit (with a large associated

database) is the Bukit Asam deposit in Sumatra. The main economic seams in the

Bukit Asam Mine were deposited during the regressive phase (Late Miocene) of the

Muara Enim Formation in the foreland (back arc) zone of the South Sumatra Basin

(Fig. 7.7). During coal deposition the basin was essentially stable with a regular

pattern of subsidence (Kinhill-Ottogold, 1984). This condition allowed the seams to

be deposited with a relatively regular distribution.

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On a coalfield scale, several features are quite different when the Bukit Asam

Coalfield is compared to the Sangatta Coalfield. Due to the availability of coal data

from the A l Bukit Asam coal, a detailed comparison was undertaken between the A l

seam at Bukit Asam and the Sangatta seam. Differences between the seams are

detailed below.

1. Coal thickness is more variable in the Sangatta seam. This is indicated

by the higher coefficient of variation, lower fit of the trend surface and

lower range of the variogram (Fig. 7.8).

2. Widespread clastic partings are absent from the Sangatta seam. Most

partings in the Sangatta seam were water transported and consist of

coaly shale and siltstone (probably overbank deposits. In contrast, most

partings in the Bukit Asam coals consist of pale tuffaceous materials and

the thin partings are commonly pelletoid in nature (not observed in

Sangatta Coalfield at any locality). The Bukit Asam partings are

generally widespread and are interpreted to have originated from

voleanic activity (Kinhill-Ottogold, 1984). In the Bukit Asam coals,

water transported materials, where present, are commonly shaly in

character (silty materials are absent), indicating suspension or colloidal

origins.

3. Washouts and crevasse splay deposits are common in the Sangatta coals

indicating that the seam was closely associated with fluviatile sediments.

In the Bukit Asam coal such washouts and crevasse splay deposits are

uncommon suggesting that the Bukit Asam coals were deposited in more

stable, more mature swamps, probably away from clastic activity. The

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Al seam of Bukit Asam is associated with thick mudstone (commonly

massive in nature, with clay-rich ironstone). Again this indicates a

stable and mature floodplain where wet and dry periods occurred.

4. The Sangatta peat swamp developed in a less stable setting resulting in

a less uniform seam (for example, rapid splitting and tapering). Peat

accumulation in the Al seam (Bukit Asam) was uniform (Kinhill-

Ottogold, 1984) and more widespread in the South Sumatra Basin

(Matasak and Koesumadinata, 1976).

5. The vitrinite/inertinite ratio is slightly higher in the Sangatta seam,

indicating a different level of humidity in the two peat swamps

(Cameron et al, 1989); the Sangatta peat was probably more humid and

more domed. (Petrological data from the Bukit Asam coal is from

Waluyo (1992)).

6. The telovitrinite/detrovitrinite ratio is higher in the Sangatta seam

indicating a higher degree of preservation or a higher proportion of

woody vegetation (Al petrological data from Waluyo, 1992).

From this comparison, it is suggested that the Sangatta seam appears to have been

deposited in a less stable setting and is not as widespread as the Bukit Asam coals.

The deposition of the Bukit Asam coals are probably comparable with modern peat

accumulation in eastern Sumatra . Many of the eastern Sumatran peat deposits are

flat or slightly domed, plant zonation has not been observed and some peat swamps

are subjected to flooding (Cameron et al, 1989; Esterle and Ferm, 1990; Esterle et

al, 1992). Although the role of a flat peat swamp in producing economic coal

deposits is emphasised by Diessel (1992), the eastern Sumatra peat swamps seem to

183

be less comparable with the ancient Sangatta peat swamp.

Modern analogues for the Sangatta seam should be investigated in other geological

settings such as Kalimantan, Malaysia or the United States. The high vitrinite and

low inertinite contents provide an indication that the Sangatta peat swamp may have

been located in a less stable basin (Shibaoka and Smyth, 1975; Smyth, 1980). With

respect to the raised bog interpretation, the low inertinite content of the Sangatta

seam suggests that the peat bog must have experienced a humid environment where

the convexity was the function of humidity, a feature discussed by Cameron et al

(1989). The high proportion of decomposed vitrinite implies a high temperature in

the peat swamp, where bacterial decomposition is higher than in cooler regions

(Diessel, 1992). Therefore, in seeking modern and ancient analogues for the Sangatta

seam, the above mentioned factors should be considered.

Comparisons with modern and ancient analogues.

Geographically, peat swamps can develop in cold-temperate (arctic) and tropical

regions (Stach et al, 1982; Andriesse, 1988). In terms of the geological settings,

peat swamps commonly occupy paralic (coastal) and limnic (inland) environments

(Stach et al, 1982). Most ancient peat swamps were paralic in origin (Diessel,

1984), although pure inland peat swamps are also recorded, such as present-day peats

accumulating in the Kutei Lake region, East Kalimantan, Indonesia (Flores, 1986,

1993; Moore, 1991).

In paralic (coastal) regions, peat swamps develop in various settings such as:

deltaic plains (lower to upper delta plain) such as the Fraser River

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Delta, Baram Delta, Rajang Delta, Batang Hari Delta and Klang-Langat

delta;

tidal platforms (for example, Florida Everglades and eastern Sumatra);

and

back barrier lagoons (for example, Okefenoke Swamp).

In terrestrial (fresh-water) environments, peats develop in intramontane basins, such

as the fluvial Kutei Lake system and Okavango delta, and river systems such as the

fluvial plain of the Mississippi River (Morgan, 1970; Kosters et al, 1987).

With respect to the sedimentological, geometrical, petrological and chemical aspects,

the Sangatta seam has one or more features which is/are analogous to peats

accumulating in various geological settings such as the Snuggedy peat (Staub, 1991),

Indo-Malaysia peat (Anderson, 1964, 1983; Coleman et al, 1970; Morley, 1981;

Esterle et al, 1989; Calvert et al, 1991; Dehmer, 1993; Esterle and Ferm, 1993;

Staub et al, 1991) and Fraser River Delta peat (Styan and Bustin, 1983; Styan and

Bustin, 1984). The Sangatta coal is also comparable with some coal deposits such

as the Powder River Basin coals (Moore, 1991; Flores, 1986, 1993; Warwick and

Stanton, 1988),- southern Kentucky coals (Esterle and Ferm, 1986), Middle

Pennsylvanian coal (Eble and Grady, 1990), Appalachian coal beds (Home et al,

1979; Staub et al, 1991), N e w Zealand coals (Neuman, 1989; N e w m a n and

Newman, 1992; Shearer, 1992), Durham coals (Fielding, 1984) and Mist Mountain

coals (Bustin and Dunlop, 1992).

The Snuggedy peat as described by Staub (1991) is similar to the Sangatta peat in

terms of the scales, thickness changes and morphology. The peat is slightly raised

with the thickest, low ash fresh-water swamp in the centre. The changes in

185

thickness and ash content occur over a very short distance within a small swamp

(650 km 2). The rapid change was also indicated by the bimodal distribution patterns

of the peat thickness. The Snuggedy peat, however, shows a clear change from

fresh- to salt-water from the centre (low inertinite content) to the eastern margin

where the peat is thinnest and ash yield and inertinite contents are highest; this

feature is not observed in the Sangatta seam.

Staub (1991) compared the Snuggedy peat deposit with the Pacahontas coal bed in

the Appalachian Basin, West Virginia (USA). This coal bed occurred within the

upper portion of a sedimentary package that developed in regressive environment

changing from marine to fluvial-deltaic environments. In general, the vertical

sequence for the Snuggety peat appears to be similar to the Miocene sequence in the

Sangatta Coalfield, but it does not match the depositional environment of the

Sangatta coal itself. Using geomorphic characteristics, Staub et al. (1991) compared

the Pacahontas coal bed with the central Sarawak lowland peat deposits (near the

Rajang Delta) Malaysia. A significant feature shown by the two deposits is the

control of syn-depositional faults (perpendicular to the clastic depositional direction)

on the thickness distribution. The thickest coal is localised in the topographic lows

on the Pacahontas peat platform; this is not comparable to the Sangatta seam where

the upthrown side of the major growth fault has occupied by thickest coal.

The Indo-Malaysia peats are generally raised bogs. Studies of raised-bog peat

deposits (Anderson 1964, 1983; Anderson and Muller, 1975) showed that:

(i) zoning in the raised bog vegetation is characterised by

a peripheral zone with taller, bigger and luxuriant plants, and more

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species, and

the central zone with shorter, smaller and stunted herbaceous plants,

fewer species and sphagnum a diagnostic plant.

(ii) areal zonation of the vegetation which affects the vertical variation of

the peats resulting in

humified woody peat and nutrient-rich peat in the lower part, and

less humified, fibrous peat in the upper part.

Studies of the internal structure, stratigraphy, petrology and geochemical composition

of the Indo-Malaysian peats (Coleman et al, 1970; Morley, 1981; Esterle et al,

1989; Calvert et al, 1991; Dehmer, 1993; Esterle and Ferm, 1993) confirmed that

plant zonation is a feature of domed peats. These studies also suggested that vertical

variation in peat petrology is only significant for vitrinite pre-macerals and this led

Esterle et al. (1989) to their conclusion that there would be no 'dulling-upward' in

the Indo-Malaysian tropical raised bog coals. The pre-vitrinite maceral variation

(fibric peat in the upper and central parts, woody peat in the middle part and sapric

peat in the lower part and margins) was controlled by three major factors - botanical

input, degree of preservation and burial preservation (Esterle and Ferm, 1993).

Most of the peat deposits in the Indo-Malaysian region are characterised by low ash,

low sulphur and the absence of widespread clastic partings (Coleman et al, 1970;

Esterle and Ferm, 1993). High sulphur content in the lowermost parts of most Indo-

Malaysian peat was reported by Esterle and Ferm (1993) and this is a result of peat

accumulation on a progradational deltaic settings which commenced with brackish

peat (Coleman et al, 1970; Esterle and Ferm, 1993). This is not comparable with

187

the characteristics of the Sangatta coal, because most bottom samples of the Sangatta

seam have a low sulphur content, probably indicating fresh-water initiation. In the

Baram River swamp, Esterle and Ferm (1993) reported that the peat body is most

continuous parallel to the trunk rivers and this is comparable with the thickness

distribution in the Sangatta seam. Although Moore (1987) noted that many peat

swamps developed from low moor to raised bog, as recorded from European peat

successions (for example, from lake clays to swamp and fen peats to wood peats to

sphagnum peat), the Indo-Malaysian raised bogs generally started with non-lake

organic deposits (Esterle and Ferm, 1993).

Styan and Bustin (1984) studied peat deposits in the Fraser River Delta, British

Columbia, Canada. They described peats from several sedimentary settings including

alluvial plain, transitional settings between upper and lower delta plains and distal

lower delta plain. The authors discussed hypothetical seams likely to develop in

each of the above geological settings. The hypothetical seam for the alluvial plain

(Pitt M e a d o w swamp) would have similar geological parameters (thickness, isolated

and laterally restricted, low ash and sulphur contents) to the Sangatta seam.

However, types of vegetation developed in the two peat swamps were significantly

different; Pitt Meadow vegetation was less woody whereas Sangatta peat was derived

from arborescent (dicotyledonous) vegetation. This is probably a function of the

climate for the two swamps (temperate in the Fraser River Delta and tropical in the

Sangatta swamp).

Among ancient peat deposits (coals), the Powder River Basin coals have a well-

defined depositional environmental model. The coals were deposited within an

intramontane basin (Flores, 1986, 1993). Many of the coals were deposited in raised

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swamps on floodplains of meandering and anastomosing river systems as indicated by

an upward-decrease in the telovitrinite/defrovitrinite ratio due to a decrease in woody

vegetation toward the top of the peat (Warwick and Stanton, 1988; Flores, 1993, Fig.

7.10). Moore (1991) modelled the mechanism of seam splitting in the Powder River

Basin and found the following sequence:

(i) peat was initiated on a flat substrate (Dietz #1 peat);

(ii) most of the peat body was not reached by clastic sediment due to

doming;

(iii) after subsidence of the eastern part of the swamp (by differential

compaction or fire), the low area was inundated with thick clastic

sequence which provided greater compaction of the underlying peat; and

(iv) with the clastic sedimentation the eastern part became less compactable

and re-established a new peat swamp (Anderson peat).

The depositional model for the Powder River Basin coal appears to be similar to the

Sangatta coal, especially in terms of the geometry and quality parameters. However,

the tectonic environment of the two coals seems to be different as the Sangatta coal

was not deposited in an intramontane basin.

Depositional models related to thickness and coal quality variations have been studied

for the Allegheny deltaic coals (Home et al, 1978; Ferm and Staub, 1984). It was

suggested that thickness variations were controlled more by abrupt seam splitting due

to inundation and peat redevelopment rather than channelling. The role of

compactability on the substrate sediments governing the coal thickness variability was

emphasised and is was stated that optimal peat accumulation would be in areas

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having a balance between compaction and peat growth. It was suggested that peat

morphology was related to coal quality characteristics with split coals having higher

sulphur and ash and lower vitrinite content. Compactability of substrate sediments

was also postulated as one of the factors controlling the geometric development in

the Sangatta peat. However, the relationship between splitting and sulphur, and

vitrinite contents, is not seen in the Sangatta seam.

In the Hance seam (Breathitt Formation, southern Kentucky), Esterle and Ferm

(1986) suggested that the thick coal had low ash and sulphur contents. A low

vitrinite content in this zone was due to a low proportion of large tree vegetation.

'Dulling-upward', noted in the thick seam, was interpreted as the result of doming

where the highest part of the peat was subjected to oxidation. The opposite features

were found along the split marginal seam. Some of these coal characteristics are

comparable with the Sangatta seam. The differences between the Hance and the

Sangatta seams relate to vegetation types and the 'dulling-upward' in the peat. The

Sangatta coal is always bright and large trees remain dominant in the thick non-split

zone of the Sangatta seam as well as around the margins. This may also relate to

different climates for the development of the two peats.

In the Durham Coal Measures (northeastern England), Fielding (1984) noted that:

(i) coals were deposited on part of a broad, flat deltaic plain which

prograded southward;

(ii) regional depositional features of the seam were governed by major delta

switching;

(iii) local seam geometry was controlled by local sedimentary processes and

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subsidence patterns;

thick and laterally extensive seams commonly developed on the upper

delta/fluvial plain; their development was controlled by a balanced rate

of subsidence and peat accumulation in areas underlain by non-channel

deposits; and

this model is not compatible with the coastal plain models of

Appalachian region proposed by H o m e et al, (1979).

Some of the criteria documented by Fielding (1984) are observed in the Sangatta

seam, especially the control of sedimentary processes and subsidence on the local

variation of seam geometry.

The control played by clastic depositional environments on thickness and quality

variations in coal was discussed by Bustin and Dunlop (1992) for the Late Jurassic-

Early Cretaceous Mist Mountain Formation seams, southern Canadian Rocky

Mountains. These authors suggested the roles of substrate and contemporaneous

sediments were to govern coal thickness variability. For example, the influences of

contemporaneous and subsequent channels consistently reduced or modified the seam

thickness. Similar sedimentary features are also observed in the Sangatta seam where

differential compaction and channelling clearly controlled the thickness distribution

and its variability.

The controls of the depositional environment on the thickness and quality variations

were also reported for some N e w Zealand coals (Newman, 1989; Shearer, 1992).

These authors suggested that aerobic decomposition caused an increase in

detrovitrinite (low TPI) toward the top and the centre of seams where ash yield was

(iv)

(v)

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low. They coiifirrned this type of degradation by the negative correlation between

the degraded vitrinite content and the mineral and sulphur-free volatile matter

contents. For the Sangatta seam, however, this kind of relationship seems to be

difficult to assess because spatial changes in coalification level have obscured the

relationship.

Discussion

Many of the geological characteristics of the Sangatta seam are analogous to one or

more features of the various m o d e m and ancient peat deposits. The extremely low

ash yield and low sulphur in the Sangatta coal are correlated with raised bog peats

that accumulated in paralic and terrestrial settings. The high vitrinite content, derived

from woody tissue, is similar to the typical arboreal vegetation in most tropical peat

in Indo-Malaysian swamps. The spatial variations in the vitrinite macerals shown by

the Sangatta coal can be explained by the vegetational zoning in most of the m o d e m

peat analogues. The zone of the Sangatta seam with highest continuity parallels the

main palaeocurrent and this is comparable to some fluvial or upper deltaic coals

which are more persistent in the depositional dip direction. However, the high

degree of thickness variability of the Sangatta seam is apparently not relevant to any

of the m o d e m and ancient deposits but this may be due to a lack quantitative

information about such variability in the m o d e m and ancient anologues, rather than

an overestimation of the Sangatta seam thickness variability.

Most differences between the Sangatta seam and the individual modem and ancient

analogues can be attributed to factors such as climate, type of vegetation, and

patterns of variation in the vitrinite macerals and quality parameters. The extremely

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vitrinite-rich Sangatta coal is not comparable to modem and ancient peat deposits

from temperate and dry climate regions. The significant amount of dicotyledonous

woody tissues in the Sangatta coal cannot be correlated with most pre-Tertiary

ancient peats. Although the pre-vitrinite-rich peat of most tropical modem deposits

is similar to the Sangatta coal, the former commonly shows concentric zoning with

regard to peat composition. The low sulphur at the bottom of the Sangatta coal is

inconsistent with many modem peat deposits which have accumulated in prograding

deltaic environments.

The detailed depositional system of the Sangatta seam is unique when compared with

the modem and ancient analogues. The seam was mostly deposited as fresh-water

peat on a fluvial floodplain setting. In the last stage of the accumulation, the

southern part of the seam was inundated by marine or brackish water which

increased the sulphur content toward the top of the seam in that area. This suggests

that a sea level rise occurred during the deposition of the uppermost part of the seam

and it also indicates that the Sangatta peat swamp was then under a marine

influence, that is, it probably accumulated on a fluvio-deltaic plain.

The control effected by differential compaction, splitting and washouts on the

geometry and thickness variations of the Sangatta seam is comparable to that found

in some ancient analogues. Differential compaction was also responsible for

initiating local morphologic variations which in turn caused variations in hydrologic

conditions and ultimately variations in plant input and preservation/degradation

conditions. This is reflected in the spatial variation of the maceral contents in the

Sangatta seam. The petrographic data suggest that the depositional setting of this

coal is comparable to modem tropical forest peat of the Southeast Asian region

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where the humid climate, peat vegetation and preservation/degradation conditions

appear to be equivalent.

Coal petrographic data suggest that a modified Diessel TPI-GI diagram can be

applied to compare the depositional environments of Tertiary Indonesian coals, but

the environments are not comparable to those of the Permian coals because of the

major difference in climate and plant types. For the Indonesian coals, the TPI-GI

variation can be attributed to humidity levels, degree of doming of the peat bog and

pH conditions. For example, the Sangatta coal generally shows higher TPI and GI

values compared to the Bukit Asam coal indicating that the former accumulated in

more humid, more domed and lower pH conditions.

Development of the Sangatta peat swamp was controlled by several major factors.

1. Condition of underlying strata controlled the configuration of the peat floor

with physical characteristics of the rock (compactability, subsidence, differential

compaction and growth faults) playing an important role in establishing the peat

platform. *

2. Climate (humidity, rainfall and temperature) controlled the degree of doming,

oxidation level (formation of inertinite) and microbial activity (decomposition

rate).

3. The water table and drainage controlled the distribution of vegetation types,

base level fluctuation (preservation-degradation level) and pH conditions.

4. Subsequent syn-depositional processes, such as self-compaction and erosion,

modified the geometry of the peat.

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The high detrovitrinite content in the central zone of the Sangatta seam can be

attributed to two major factors.

1. From a chemical viewpoint, high pH enhanced bacterial (decomposer) activity

and aerobic conditions increased aerobic decomposition. Dead plants would be

easily decomposed in very wet swamps where p H was high or in swamps with

a very low water table.

2. From a plant type viewpoint, soft tissues of herbaceous plants which grew in

the central zone of a raised bog characterised by a low water table, would be

more easily decomposed (mostly by aerobic decomposer) and, therefore, the

particulates of the detrovitrinite matrix would be mainly from this kind of

vegetation (Diessel, 1992). Extended humification processes also caused woody

tissues to decompose (Diessel, 1992). For this type of vegetation, different

parts of plant tissues would degrade differently as shown by Glikson and

Fielding (1991) who stated that accumulations of leaves (rich in lipids) are

more easily degraded than woody tissues.

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CHAPTER EIGHT

FACTORS GOVERNING RESERVE

ESTIMATION

8.1 CONCEPTS IN RESERVE ESTIMATION

Several concepts were considered in the past when developing mineral reserve

estimation systems. They were summarised into the concepts of earth crust, geology,

economic geology, mining economy, and mineral deposits (Fettweis (1979). These

concepts reflect the development of the thoughts of geologists and mining engineers

who were concerned with mineral resources.

In the earth cmst concept, unlimited mineral occurrences were believed to be present

in the earth and, therefore, there is no concern about the amount of reserves. In

contrast, the geological concept introduced the terminology 'deposit' and 'resources'

whose distribution are controlled by geological conditions. In this concept geological

knowledge is needed to locate mineral deposits. However, the mineral deposits and

resources will not have economic values without the techno-economic considerations

of the deposits. This led McKelvey (1973) to propose a new concept called the

economic geology concept. This concept was introduced as a compromise between

geologists and mining engineers. In the economic geology concept, mineral deposits

are weighted with the economic values. Here, a new terminology 'reserve' was

introduced. The other two concepts, mining economy and deposit concepts, were

concerned with the prospect of mineral deposits in the future. The mining economy

concept considered mineral deposits in relation to current and future technological

196

and economical conditions. The deposit concept utilises the fact that most mineral

deposits must, one day, be exhausted; this would be after the production life time.

In the last three decades, concern has been expressed about the environmental

impacts (both in eco- and socio-systems) of mining activities. The negative effects

of mining on the physical and social environments have been translated by

economists into environmental costs. In some countries, legal conditions concerning

development and environmental planning, and land rights, are also considered when

planning mining activities. This has increased the number of factors that have to be

considered in any study of mineral reserves.

8.2 FACTORS IN COAL RESERVE ESTIMATION

Many reserve estimation and classification schemes have involved most of the factors

outlined in the previous section. The USGS reserve estimation and classification

system, for example, has been continuously improved and ratified by adding new but

related factors. The last version of the USGS coal reserve estimation and

classification system (Fig. 8.1) was proposed by Wood et al (1983). In this version,

locality, and environmental and legal factors have also been considered and this has

provided more control for coal reserve classification. These new factors can be

included with the factors of technology (mining) and economy (cost and revenue).

An excellent discussion about the assessment of coal reserves was given by Ward

(1984). This author delineated, systematically, the major factors that govern any coal

reserve estimation and classification including geological certainty, minability and

marketability (Figs 8.2, 8.3). Ward's first diagram (Fig. 8.2) gives a step by step

sorting of coal resources to the level of marketable coal reserve using three major

197

factors. According Ward (1984), any coal reserves have to be:

(i) certain geologically;

(ii) minable; and

(iii) marketable.

If these criteria do not all fit for any coal deposit, it should only be categorised as a

coal resource (Fig. 8.3).

Wood et al. (1983) and Ward (1984) elaborated the geological, technological and

economical factors to be applied in any coal reserve classification system. The

geological certainty (geological assurance) is controlled by the complexity of the

geometry and quality distribution of the coal deposits. Different degrees of

complexity would require different spacing of information points to model the

deposit. Based on the degree of geological certainty, Wood et al (1983) and Ward

(1984) categorised coal deposits into five different levels from high to low degrees of

certainty respectively, measured, indicated, inferred, hypothetical and speculative

resources. The authors used information points with a 1 km spacing as the minimum

distance between data points for the resource to be given as a demonstrated resources

(measured and indicated). However, because of differences in depositional

conditions, this distance cannot be applied universally for all coal deposits.

Consequently, the criteria used to classify coal resources are not only restricted in

any particular country to suite the needs of that country, but also have to be adjusted

according to geological characteristics in a particular coal basin.

For demonstrated resources to have an economic value, and thus be classed as coal

reserves (Fig. 8.3), the resources have to be at least conceptually minable and

198

marketable (Fig. 8.4). The economic minability and extractability or workability of a

coal deposit is defined by several factors such as the geographical location and extent

of the deposit, legal and environmental conditions, thickness, depth, dip of the strata,

roof and floor rock conditions and ground water conditions of the deposit. The

marketability is controlled by the quality (for example, ash yield and sulphur content)

and amount of the coal.

Although the conditions of the geology, minability and marketability of coal deposits

vary throughout the world, the concepts expressed by Wood et al. (1983) and Ward

(1984) can be applied universally in any coal region. However, the weights and

magnitudes assigned to various parameters should be justified according to the local

conditions.

8.3 DEPOSITIONAL MODELS IN COAL RESERVE ASSESSMENT

Although coal is considered one of the most continuously distributed type of deposits

(King et al, 1982), in many cases the thickness and quality vary quite markedly. To

extract coal economically from such seams, the reserve must be defined accurately.

Because most coal reserve estimations involve errors, the tasks of the exploration and

mining geologists are, therefore, to minimise the errors of estimation.

The errors of estimation are usually influenced by the degree of geological certainty

of coal deposits and are determined by the density of the data points and complexity

of the coal deposits. In coal resource assessment, depositional models of seams have

a twofold benefit. Firstly as a guide for predicting the lateral extent of the seam

and, secondly, as a tool to improve understanding about the spatial variations of the

199

thickness and quality of the coal deposit

Depositional models provide guidance when designing the exploration strategy of coal

deposits. For example, drilling density in new areas that have similar depositional

environments (especially in the same basin) can be determined using the existing

models. The depositional models would also be beneficial for increasing geological

certainties in coal reserve classifications and estimations. As a qualitative tool, the

models determine the complexity of the geometry and quality of seams and provide

significant direction and awareness in using any reserve estimation techniques.

Home et al. (1978) discussed the significance of depositional models in coal

exploration and mine planning.

Coal reserve assessments involve determination of the amount, quality and

technological conditions of coal deposits. Depositional models provide a conceptual

explanation for the variations in coal thickness and quality, and floor and roof rocks

types.

Depositional models and geological certainty

Geological certainty of coal deposits is mainly determined by the geometry and

thickness variations of the seams studied. Factors that commonly control thickness

variations are lensing, washouts, splitting, faults (including growth faults) and burning

(fire). Detailed studies of seam depositional environments model the geometry of the

seams and locate the geological elements that govern the thickness variations. Based

on the depositional model the optimum density of drillholes and sample points can

be designed.

200

In the Sangatta Coalfield, the details of the depositional environment of the Sangatta

seam has been modelled in an integrated study of sedimentology, coal petrology and

statistical analysis of the thickness and quality data. The four zones with different

seam geometry and thickness characteristics also differ in their statistical parameters.

Thus, each should have different criteria used in its reserve classification and

estimation.

In the western and northern zones the seams are thickest and more uniform than

elsewhere. For estimating the amount of coal in these zones, a low density of data

points can be used. In contrast, the central and eastern zones need a higher data

density because the geometry of the Sangatta seam in these areas is more complex.

In addition, the strong anisotropy of the seam distribution in the central and eastern

zones needs a directional strategy in the reserve study. Therefore, to obtain the same

level of errors and confidence level, each zone needs to be assessed by different

criteria.

Depositional models and minability

The degree of minability of coal deposits is determined by several factors, including

geological elements such as thickness and geometry (thickness variations) of the

seams, dip, geomechanical and hydrological conditions of interseam strata and depth.

Depositional models delineate the geometry and thickness variations of seams. The

models also provide general information related to the rock properties of overburden

and floor strata.

201

In the case of the Sangatta seam, the western and northern zones have a higher

degree of minability for several reasons:

(i) the seam does not split

(ii) the seam is more continuous and has a more regular geometry;

(iii) faults are less developed; and

(iv) geotechnical conditions of the overburden and floor rock are quite good.

The western and northern zones can be developed both by open pit and underground

mines. Although the company has commenced mining activities in the Sangatta

seam from these zones by using a conventional truck and shovel method, bucket

wheel excavators (BWE) may also be suitable because of the regularity and

continuity of the seam, the stability of the interseam rocks and the lack of sandstone

bodies (hard bodies) in the overburden strata of these zones. In places with very

thick overburden, where surface mining is no longer economic, underground mines

can be developed. Although a long wall method may be applied in these western

and northern zones, a board and pillar method is thought to be more suitable because

of the limited extent of the regular part of the seam.

The track and shovel mining technique, as already applied by the company in most

pits of the Sangatta Coalfield, is extremely appropriate in the central and eastern

zones. This is because of the higher flexibility of the truck and shovel technique for

overcoming the complex geometry of the seam (Ward, 1984) and the highly variable

overburden materials in these zones. In the northern part of the central zone, where

the overburden is thick, underground operations would be difficult because of the

complexity of the seam geometry and syndepositional structures. In the eastern zone,

there is no necessity for underground mining because of the thin overburden.

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Coal utilisation and marketability

When a coal deposit is suitable for mining, the utilisation and marketability of the

deposit are then determined by the chemical and physical properties of the coal. As

some of these chemical and physical properties can be assessed by the depositional

environment of the coal seam, studies such as this one have important, indirect

consequences for utilisation and marketing.

Coal utilisation and trade are dominated by two major types of coal, steaming and

coking coal. Steaming coal is usually used as a fuel whose quality is determined by

several parameters such as calorific value, ash yield, ash composition, ash fusion

temperature, sulphur, moisture content, and to some extent, maceral composition.

A good coking coal produces a high coherent carbon residue when coked and must

have caking properties when heated to a specified temperature (Ward, 1984). The

caking properties are controlled by the chemical and maceral composition and the

rank of the coal; this is partly reflected in the Crucible Swelling Index.

In the steel making process in blast furnaces, cokes are used as the fuel, the reducing

agent and the support for other materials (Cook, 1973). As a fuel, coke must have

properties at least similar to steaming coal. As a reducing agent, coke has to have a

high porosity and permeability; these properties are related to the textures and

structures of coke which are controlled by the proportion of reactive constituents

(vitrinite and liptinite) and rank of the raw coal. Coking coal has to be able to

produce coke with an optimal strength. Coke strength is assessed by measuring the

hardness and stability of the coke - the most important properties use to distinguish

203

coking from non-coking coal. Two parameters controlling the stability and hardness

of coking coal are maceral composition (50-60% vitrinite, 30-40% inertinite) and

rank of the raw coals (0.9%-1.6% vitrinite reflectance or bituminous coal rank).

The Sangatta coals do not have good caking properties, as reflected by the low

swelling indices (1 to 1.5). This is probably due to the low rank and very low

inertinite content of these coals. Thus Sangatta coals are more suitable as a steaming

coal but can be used as a minor blend component for coke.

The ash yield is lowest in the western zone and the run of mine coal from this zone

is the cleanest coal in the coalfield and does not require washing. This coal can be

blended with high-ash coal from other zones to produce a uniform quality coal.

The sulphur content is lowest in the central zone and gradually increases towards the

peripheral zones. Most sulphur values are below 1% and it is not necessary to blend

coals to minimise sulphur content.

Although rank shows a gradual change across each zone (highest in the central and

eastern zones), economically the variation is not significant.

8.4 REVIEW OF RESERVE ESTIMATION IN THE SANGATTA

COALFIELD

Methods of reserve estimation

Several methods have been employed by mining geologists to estimate coal reserves.

204

They may be categorised into 2 systems namely conventional or geometrical methods

and mathematical methods.

The geometrical methods, such as polygonal and triangular methods, have a simple

concept of extension as the basic principle; the value of a variable obtained from

drillholes is assumed to be constant over the entire block. These methods, which use

only very simple arithmetic calculations in the reserve estimation, were the most

commonly-used methods until the advent of computers, and are still favoured by

many companies (David, 1977); they are less appropriate for complex coal deposits.

As far as local estimation is concerned, these geometrical methods are very poor

because they do not take into account the structure of the deposit (Guibal, 1984).

The mathematical methods apply statistical theory and mathematical equations to

obtain estimated values for each geological parameter. T w o basic concepts used in

most mathematical methods are weighting and searching. Weighting assigns a set of

weights to each sample according to the relevance of the respective points or blocks

being estimated. Searching selects data used in the estimation procedure. The area

of searching can' be spherical or elliptical and the choice of either, generally depends

on the estimation techniques used and the isotropy of the coal deposit. The

techniques of weighting and searching vary according to the statistical methods being

used.

In the inverse distance weighting method (one of the weighted moving average

techniques), the estimated values of grids or blocks are calculated from the data

surrounding these grids. The nearby data are assigned a greater weight than a point

farther away from the grid point. Powered inverse distance is commonly used in

205

coal reserve estimation where the particular weights are inversely proportional to a

power of the distance. The distances are calculated from grid points or from the

central points of blocks under consideration. The decision as to whether or not the

distance should be squared or cubed is based on past experience and is quite an

arbitrary one (Baafi, 1981). Most of distance weighting methods normally employ

spherical areas when searching for sample points that are to be used in the

estimation because the spatial structure of the data are not taken into account.

In Kriging, the best set of weights is found according to the geometry of the

problem and the character of the deposit so as to minimise the estimation variance.

The geometry and character of the deposits (reflected by the spatial structure of the

data) are defined by variogram analysis. The parameter values of the variogram are

used to solve the kriging linear equation. In order to be an unbiased estimator, the

sum of the weights is set at 1. As an exact estimator, kriging assigns estimated

values at the sample points and these are taken to be the actual values. Another

important property of kriging is that the results are conditionally unbiased (David,

1977; Baafi, 1981). Although kriging is commonly termed the best linear unbiased

estimator (BLUE), the accuracy of kriging results is defined by the quality of the

variogram analysis that is a major part of any geostatistical work.

The searching techniques of kriging (sorting) use two concepts, selecting and

filtering. Selecting is used to decluster the data and to limit sample points based on

the area of influence. Filtering screens the influence of sample points situated

behind points that are closer to the estimated points or blocks.

In trend surface analysis, no special weighting or searching technique are employed

206

because the estimated values of grid nodes are calculated on the basis of the

polynomial equation generated from the entire data set (Chapter 6). Although several

commercial mine planning programs offer trend surface analysis as a griding option,

trend surface is only suitable for modelling large-scale trends rather than modelling

small-scale variations (Knudsen, 1985). Moreover, trend surface analysis is only

suitable for coal deposits which lack local fluctuations of the parameter being

analysed (Armstrong, 1981).

Existing reserve estimation method by the company

The mining geologists of P.T. Kaltim Prima Coal (KPC) employ the Height method

to estimate coal reserves in the Sangatta Coalfield. This method is a combination of

the first order trend surface and powered inverse distance techniques developed in the

Mincom geological modelling computer package (Miner2). A similar technique is

also available in the griding and contouring software (Gridzo) of the Rockware

computer package under the moving weighted least squares ( M W L S ) griding option

(Rockware Incorporated, 1991).

The major difference between the Height method and a trend surface analysis is that

in the former, all data used in the calculation of an estimated point are weighted

inversely to the powered distance to the point, before generating the regression

equation by the least squares technique. With this technique, therefore, difference

equations are used to calculate difference grid node values.

This Height or MWLS method was shown by Mincom to be quite a robust estimator

for continuous, smoothly changing surfaces. This method has produced contour maps

207

that more closely honour the control points when compared to the inverse distance

methods (Rockware Incorporated, 1991). However, like the inverse distance methods,

the Height method does not provide confidence indicators to measure the accuracy of

the result.

The Sangatta seam varies in thickness and quality parameters quite markedly. The

zoning and high variability of the thickness should be considered in any method used

for coal reserve estimation. Conventional methods (for example, polygonal and

triangular methods) are unlikely to be used in reserve estimation because the data

carry a complex spatial structure. The same problems would also be encountered if

trend surface analysis and inverse powered distance are used for estimating the

Sangatta coal reserves. Therefore, the best method is kriging, but the zoning must

also be considered.

8.5 PROPOSED COAL ESTIMATION METHODS

One of the most suitable methods for estimating the Sangatta coal reserves is Zoned

Kriging. This method was developed by mining geologists of Amax Exploration

Incorporated, Golden Colorado (Noble and Ranta, 1984). One of the most distinct

features of this method is the use of the geologist's interpretation of geological

zoning in the kriging processes.

In the case of the Sangatta seam, the depositional model may be used to control the

steps in the geostatistical analysis. The procedures of zoned kriging can be

elaborated into 5 main steps - depositional model, collecting data from each zone,

basic statistical analysis, variogram analysis of each zone and combined zones, and

208

Kriging in each zone. A comprehensive method for the proposed reserve estimation

is given in Appendix 8.1.

The depositional model delineated 4 zones in the Sangatta seam. Each zone is

unique in terms of the thickness and related quality parameters. Basic statistics and

variogram analyses for each zone indicate the importance of different statistical

parameters. The Sangatta seam in the western and northern zones has a higher

degree of continuity and isotropy whereas in the central and eastern zones the degree

of continuity and isotropy is lower. Therefore, the variogram function cannot be

generalised for use in kriging the whole Sangatta Coalfield and reserves must be

calculated for each zone separately.

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CHAPTER NINE

CONCLUSIONS

The study is a review of the Sangatta seam which is the most important seam in the

Sangatta Coalfield, Kalimantan, Indonesia. As this coalfield has already been

explored in detail, it has a large data base for statistical analysis and modelling of

coal seam geometry and coal properties. The models resulting from this study will

be applicable to other seams in this coalfield and to other coalfields in Indonesia, at

least in those basins which have similar geological conditions.

Coal reserve estimations are related to the spatial aspects of thickness and quality

parameters of the seam. Therefore, any improvement in the geological knowledge of

these parameters will be of particular benefit to a country that is focussed on

improving coal production.

An integrated approach comprising geological and statistical (qualitative and

quantitative) analyses was applied in this study. The method included analyses of

geological maps,'measured sections, lithologs, geophysical logs, outcrop features and

coal petrology. Quantitative analysis, consisting of basic and spatial statistics, used

coal thickness and quality data from proximate and ultimate chemical analyses.

The major objectives of the study were to interpret the depositional environments of

the Sangatta seam; to use the depositional model in geological assessment of the coal

seam, basin analysis, reserve estimation systems, mine planning and coal utilisation;

and to contribute to the study of depositional systems and reserve classification and

210

estimation of coal deposits.

9.1 CONCLUSIONS

The main conclusions resulting from this study are listed below.

1. The Sangatta coal seam which has an average thickness of 6 m, was

deposited in a mixed-load fluvio-deltaic sedimentary system in the

Middle-Late Miocene Balikpapan Formation, northern Kutei Basin,

Indonesia. Palaeocurrent data and the patterns of the sedimentary facies

changes indicate that the main transport direction was to the southeast.

2. Local changes in the sedimentary facies occur across the Sangatta area

and indicate an immature fluvial sedimentary setting. This resulted in

instability and morphological variations across the Sangatta peat-forming

platform.

3. The Sangatta peat swamp was juxtaposed against fluvial channels which

were active sites for clastic sedimentation. The channels show a

meandering character, but in their development some of the channels

were stabilised by the vegetated levees and overbank areas. Channel

migration and shifting was retarded, resulting in low sinuosity channel

types. Migration of the channels was controlled by local differential

subsidence in the peat swamp, which caused periodic avulsion.

4. Most clastic partings and washouts in the Sangatta seam are related to

211

the fluvial sedimentation.

Syn-depositional deformation such as differential compaction and

differential rates of local subsidence, together with the clastic

sedimentation caused splitting in the Sangatta seam, with the Middle

seam in the central, eastern and northern areas being the upper split of

the Sangatta seam.

Variations in local morphology and hydrologic conditions controlled

mineral contents in the peat and later the coal. The coals are

characterised by a high vitrinite (average of 91%), low liptinite (average

of 3%), low inertinite (average of 3%), very low mineral matter (average

of 2%) and low sulphur (average of 0.4%). This has been interpreted as

the result of doming of the peat to form a raised bog and, at some

stages, confinement of river channels by the vegetated levees.

Variations in local morphology and hydrologic conditions are also

reflected by the zoned distribution patterns of vegetation types and

preservation/degradation characteristics in the Sangatta peat swamp.

This is inferred from the spatial variations of vitrinite macerals across

the coal seam. But as a whole, the very high vitrinite content (average

of 91%), very high vitrinite to inertinite ratio (30:1) and lack of fusinite

in the Sangatta coal suggests a humid climate during peat accumulation.

The petrography of etched coal provided better results as it shows

botanical structures and preservation/ degradation signatures of vitrinite

212

macerals better than in unetched samples. With this technique it was

possible to distinguish woody tissue from other plant tissue. Because

different vitrinite precursors have different degrees "and rates of

preservation, the etching technique has improved the precision of the

tissue preservation/ degradation concept. In addition, the wood textures,

revealed by etching, were comparable with tropical modem plants from

Kalimantan.

The Sangatta seam has been divided into four geographic zones in

which the coals are petrographically different for each zone. The coals

of the western zone contain more wood and better preserved tissues; the

coals of the central zone have the lowest wood content and the most

degraded tissues; the coals of the eastern zone have a small amount of

wood and moderately well preserved tissues); the coals of the northern

zone contain moderate amounts of wood and moderately preserved

tissues.

Sangatta coals contain only a very small inertinite content but a very

high vitrinite content When they are plotted on the Diessel's

Gelification Index-Tissue Preservation Index diagram, they plot as a

marsh environment, which is quite incorrect, when other factors are

considered. The Diessel's diagram is based on the concept that

inertinite and specific vitrinite macerals indicate low gelification.

However, for the Sangatta coals, etching clearly shows that some

macerals, regarded as having low gelification using normal petrographic

techniques, do not have low gelification. When combined with the low

213

inertinite contents, this overestimates the degree of gelification. To

overcome these problems:

(i) it is necessary to plot the maceral compositions as determined

from etched samples; and

(ii) the gelification index should not rely only on the vitrinite/

inertinite ratio but should weighted towards the ratio of vitrinite

types.

11. Rank determined from vitrinite reflectance (Ryinax), calorific value and

volatile matter content indicates that the Sangatta coal can be classified

as sub-bituminous to high volatile bituminous coal. Rank increases

eastward, as does the depth of the burial, towards the Pinang Dome and

Makassar spreading centre. Decreased vitrinite reflectances and

increased volatile matter and sulphur contents in the uppermost part of

the seam profiles in the southern area, indicate sea water incursion

during the latest stage of peat accumulation.

12. Considering, seam thickness, ash and sulphur data, sulphur shows the

highest variability (coefficient of variation = 0.67), but in terms of a

spatial context, the sulphur data has the most regular pattern as indicated

by the high R value of 0.82 and by the high range value of 1300 m.

This trend was controlled by the spatial variations of the sulphur content

at the top of the seam due to a brackish water-sea water influence.

13. The thickness of the Sangatta seam shows a bimodal normal distribution

with high variability, a low degree of regularity (R = 0.36), and a low

214

degree of spatial continuity with a range of influence of 420 m. These

features indicate that the Sangatta seam formed in two stages - an initial

peat formation stage with uniform or predictable thickness variation

followed by modification of the thickness by subsequent geological

process such as erosion (washouts) and faulting.

The spatial distribution of the thickness is anisotropic with the greatest

continuity of thickness in a southeast direction (135°). This orientation

is the same as the direction of clastic sedimentation in this area.

There is a negative statistical correlation between the local mean of

thickness and the thickness variability, that is, the thickest parts of the

seam have less variation in thickness than the thinner parts. The

thickest section of the Sangatta seam is where it is not split and is

characterised by a higher content of structured vitrinite, a unimodal

thickness population, a more regular and higher degree of isotropy of

the thickness, and a low ash content. The reverse is true for the section

of the seam that is split.

The four geographic zones of the Sangatta seam have different statistical

characteristics for the coal data. The western zone has the thickest coal,

unimodal thickness and sulphur populations, smallest thickness

variability, greatest thickness continuity (range = 700 m), and greatest

thickness isotropy. The central zone has a bimodal thickness population,

a high thickness variability, a low thickness continuity (range = 300 m),

low anisotropy and a low sulphur content. The eastern zone shows the

215

greatest thickness variability with a relatively high ash yield, lowest

thickness regularity (R = 0.23) and a strong thickness anisotropy. The

northern zone generally has intermediate statistical features for most coal

quality parameters.

17. During peat accumulation the four zones of the Sangatta seam had

different depositional histories. In the central zone, peat accumulated at

the centre of a raised bog which immediately subsided and this resulted

in slowing of peat development. The western zone had the most stable

peat swamp development. In the eastern zone, although subsidence was

not as great as in the central zone, syn-depositional structures and

subsequent sedimentary processes acted on the coal seam. The northern

zone is the least known part of the seam due to minimal drilling

information. Some characteristics, such as syn-depositional structures,

washouts and coal petrography, are similar to those in the eastern zone.

18. This study can be used as a predictive model in coal exploration and

basin analysis assessment in coalfields with similar geological conditions.

Thus it should be possible to extend this study to include many other

Indonesian coalfields.

19. The depositional model resulting from this study may improve the

geological certainty in reserve estimation, mine planning and utilisation

for the Sangatta coal. The nature of the thickness and quality data for

the seam requires "zoned kriging" for coal reserve estimation and mine

216

planning. In "zoned kriging", the depositional model of the Sangatta

seam controls the steps in geostatistical reserve estimation. More

specifically, the difference in the statistical parameters in each zone

requires that variography and reserve estimation should be undertaken

separately for each zone.

9.2 FURTHER WORK AND RECOMMENDATIONS

Based on the results of this study, further work is recommended. It should now be

possible to use the statistical techniques used in this study to further our knowledge

of other Indonesian coalfields, the following are recommendations which would help

to achieve these goals.

1. Although most other economic coal seams in the Sangatta Coalfield

were also deposited in the Sangatta Coal Measures, the spatial pattern of

their seam thickness and quality parameters require further detailed

study. This study provides excellent guidelines for this future work.

2. To provide more systematic and precise temporal variations of coal

lithotypes, lithotype-based sampling is needed to determine the vertical

development of petrographic composition of the Sangatta. seam in each

zone.

3. A detailed study of reserve estimation and mine planning, guided by the

depositional model formulated in this thesis should be conducted to

improve the reliability of the reserve estimations and planning for other

217

economic seams in the Sangatta Coalfield.

4. Few studies of the magnitude of this study have been undertaken for

most Indonesian coalfields. Studies of this a type should be carried out

to provide the statistical parameters and degrees of certainty required for

resource estimation and mine planning. A standardised study should be

undertaken to compare and establish a reserve estimation system and

mining methods which should be adopted for all similar Indonesian

coalfields. The results of this study could be used as a guide for the

establishment of a country-wide reserve classification and estimation

system for Indonesia.

218

219

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Van der Heijden, E., Bouman, F. and Boon, J. J., 1994, Anatomy of recent and peatified Calluna vulgaris stemps: implications for coal maceral formation. Int. J. Coal Geol, 25: 1-25.

Wain, T. and Berod, B., 1989, The tectonic framework and paleogeographic evolution of the upper Kutei Basin. Proc. 18th Ann. Conv., Indon. Petrol. Assoc, 55-78.

Waluyo, B. H., 1992, The Assessment of Banko Barat Coal of South Sumatra as a Fuel for the Suralaya Steam Power Electric Generating Plant in West Java, Indonesia. M.Sc Thesis (unpubl), The Univ. of Wollongong, 123p.

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238

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FIGURES

FIGURES TO CHAPTER 1

240

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Fig. 1.1 Location m a p of the study area in East Kalimantan, Indonesia.

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Fig. 1.2 Coal mining carried out in seven open pit mines (coloured).

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250

251

STRATIGRAPHIC

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Mudstone, siltstone, sandstone, and coal.

Main Sangatta coal deposit containing 15 coal seams

from the Sangatta to Kedapat seams.

Coal seams typically have seat earths In the floor.

Mudstone typically shows Ironstone nodules and bands.

Sandstone bodies up to 40 m thick formed from

point bar channel sands.

Thinner silty sandstone (<1 m thick) probably

represent crevasse splay deposits.

Thick channel sandstone (10-30 m thick) In the south

of the Pinang area. The Prima and Bintang seams

form significant reserves but these seams thin

to the north where the sandstone units

become more predominant in the sequence.

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Domlnantly mudstone and siltstone Intervals with

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coralline limestone and bioturbated sandstone

In the lower part of Interval.

Fluvial sandstone with coal detritus In upper

part of Interval.

Coal seams are typically 0.5 to 2.0 m in thickness

usually with high sulphur content (>1X).

No coal of economic significance In this sequence.

Limestone, coralline, marker bed at base of

coal sequences. Mudstone with laminated calcareous

sandstone and thin limestone bands.

Fig. 2.8 Stratigraphy of the Sangatta Coalfield showing the temporal development of sedimentological associations from more marine to more fluviatile environments (from Muggeridge, 1987).

FIGURES TO CHAPTER 3

252

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Fig. 3.2 Locations of cored drillholes in the Sangatta Coalfield.

254

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Coal seam and lithologic correlation of boreholes showing widely spaced long space lateral changes of facies in clastic intervals. Locations of boreholes are in Fig. 3.7.

(A) shows a channel sand body changing the overbank deposits in the Sangatta-B2 interval in the southwest. The Sangatta-B2 interval thins to the northeast. The Sangatta seam is thickest in the middle and splits to the northeast. T w o storey channel sand bodies above the Sangatta seam are seen in the southwest. Section is sub-perpendicular to the regional palaeocurrent trend.

(B) shows channel sand bodies between the Sangatta and Ml seams in the middle of the section. Facies change from overbank splay to floodplain fine deposits is seen above the Sangatta seam. The Sangatta seam is unsplit. Section is sub-perpendicular to the regional palaeocurrent trend.

(C) shows thicker channel sand bodies above Pinang seam in the northwest and thinner channel sand bodies in the Sangatta-Pinang interval in the southeast. Section is sub-parallel to the regional palaeocurrent trend.

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Fig. 3.9 Lithologic and geophysical logs of drillhole C3486 showing a thick channel sand between Sangatta and B2 seams.

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Figure 3.21

Sandstone, (ignt-cjrsy, quartz, felspar, chert, rack fragments, sub-angular to suo rounded, grain-suported. moderately sorted, gradaflbnat from rriecxjjrrHgraneei at the base to finegrained sandstone at the top. It is paraieWammsrted. wan coal seam iraereaiatjons (0.5-1 cm th»dO tn the upper part and coat casts (up to 5 c m in diameter) in the lower part. The basal contact is sharp.

Sandstone, light-grey, quartz, felspar,chert, rock fragments, sub-angular to surxounded. gran-suported. moderately sorted, medaim-gramd, calcareous cement, 2Q c m ttnacTho basal and upper contacts are sharp.

Sandstone, light-grey, quartz, felspar, chert, rode fragments, sub-angular to sub-n-ounded, grain-suported, moderately sorted, gradatiorai from fine-drained at the base to medium-grained at the top, paralM-Hamirtated with mudstone and coal bed mtwcjUaOoiCT majjnry in the lower part.

Sandstone, white, quartz, felspar and chert, sub-angular to sub-rounded, grain-suported. weH sorted, parallel and cross-laminae, gracacoftai from medium-grained at the base to finegrained at the top. The basal contact is sharp.

CHANNEL

CREVASSE SPLAY

OVERBANK

is -J

Sandstone, light-grey, finegrained. s*y. P * ^ ™ * * watt mudstone and coal bed irtercaiations marty in the lower part, some cross4arrunae, coal and mud clasts. thn white sandstone intercalations.

Sandstone, grey, fine-grained, gradational from laminated siay mudstone w«h thin coal beds (1-2 cm) in the lower part to cross-Jamtnated st*y sandstone with coal streaks in the upper part, massive in the lower part.

OVERBANK

CREVASSE SPLAY

-V

280

Figure 3.21 (Cont'd)

Sandstone, light-grey, quartz, felspar, chert, sub-angular to sub-rounded, grain-suported, weU sorted, paraile -fairoiated in parts, coal ctasts (2-3 cm in dameter). graoiMMrtal from firw-gramed in the lower part to coarse-grained sandstone in the upper part.

CREVASSE SPLAY

Sandstone, light-grey, quartz, felspar, chert, sutwngutar to sub-rounded, grain-suported. wed sorted, cross-beds (set 10 cm, dip*30°), paraileWarrmated in the lower part, bioturbation and pUnt-fragrneras at the base, coal streaks, coal dasts (2-3 cm in diameter), gra(3ationai from very Ime-gramed in the lower part to coarse-grained sandstone in the upper part.

LAKE DELTA

"UUl/l

=3

Mudstone, grey, larmnated, plant-fragments.

Mudstone, grey to darfc-grey, rich in ptant-fragments in the upper part, saty and massive with firmthti sandstone intercalations in the rraddJe, with carbonaceous mudstone in the lower part.

F L O O D P L A I N

SiaynTiudstone, grey, massive, with siltstone irkercaiations F L O O D P L A I N WITH (cross-iarninated). C R E V A S S E S P L A Y

Shale, dark-grey, rich in plant-fragments, carbonaceous, coal B A C K S W A M P beds.

281

Figure 3.21 (cont'd)

Mudstone, grey, ptant-fragments, massive, coal beds (up to 2 O V E R B A N K L A K E cm), siay sandstone in the lower part.

Fig. 3.21 Lithologic section from drill core F5253 (Hatari Pit), s h o w i n g vertical development of sedimentary facies (bottom to top) from floodplain/lake deposits, overbank complex (crevasse splay and flood deposits) to fluvial channel deposit. The thick overbank deposit complex may indicate significant subsidence of the overbank area and high stability of the fluvial channels. Coal clasts in the middle of the channel sequence may originate from bank collapses.

282 Figure 3.22

50m

Sangaaa. coai seam, banded bright, resinous a d pyrinc most

commonly in the upper part clay band* (no. 1: nradstone, light

grey, plant-fragment*, coaly at the baa*, coarsening-upward to

silty mudstone. 30 c m thick no. 2: shaiy coaL black, dull 2 cm

thick; no. 3: coaly shale, laminated, dark grey, 5 cm thick)

Peat Swamp (Mire)

55m

60m -

Carbonaceous shale (lower part), dark grey, laminated, with

shaly coal at the top. Mudstone (upper part), grey, plant-

fragmentx.

Sandstone, light-grey, quartz, felspar, chert, sub-angular to sub rounded, jram-suported. moderaaiy sorted, gnvianrmai from coarse-grained at the base to fine-grained sandstone at the top,

btomrbated in the middle, crost-bedi and coal streaks at the base.

Tie basal and upper contacts are sharp.

Shale (lower pjarta), carbonaceous, dark grey, plant fragments,

laminated, grades into mudstone (upper parts), plant-fragments,

leaf fossils abundant at the bottom, massive, jrideriric nodule

commonly in the upper pans, thin coai beds in the upper parts.

Lake to soil

Channel

Lake to Soil

Mudstone, grey, mostly massive, plant-fragments, leaf fossil in

the lower part, sideritic nodule intercalations in the upper part,

some slkkensides at the top, thin coal bed and laminated shale in the middle part

Soil

Sandstone, grey, contains plant-fragments, fine-grained, finina-

upward to silty sandstone, lamsiflted. cross-laminated at the ba* sharp basal and upper contacts.

Crevasse channel

Figure 283

3.22 (cont'd)

65m

70m

A* ic

Siltstone. grey, plant-fragments, sandy toward the top.

Sandstone, light-grey, quartz, felspar, chert, coal clasts, fining-

upward to siltstone. cross-beds at the base (s*t-5cm. dip-15*).

plant-fragments in the upper part. The baaal and upper contacts are

sharp.

Mudstone, grey, hard, carbonaceous, massive, sideritic nodule at the

top (5 c m thick), silty in the lower part

Sandstone, light-grey, quartz, felspar, chert, clay pellets, coai clasts

(some rounded), cross-beds in the middle (sev^'.O cm, dip=25*),

biotnrbated in the lower part, coarsening-upward from fme-erained

to coarse-grained sandstone, underlain by laminated shale. The

basal and upper contacts are sharp.

Shale, grey, carbonaceous, plant-fragments, lamina- ted, leaf

fossils, grade toward the upper pan into massive mudstone wsh

sideritic nodules (3 a n thick).

Mudstone, grey, mostly laminated, leaf fossils, plant-fragments

(anenaay of carbonaceous material increases upward), grade

toward the uppermost part into massive mudstone with sideritic

nodules (up to 4 c m thick).

Floodplain

Crevasse channel

Floodplain to soil

Crevasse splay

Lake to soil

Lake

22 Lithologic section from drill core F5304 (E-West Pit), showing vertical development of sedimentary facies (bottom to top) from flood basin/lake deposits, overbank (crevasse splay, overbank channel, floodplain deposits) to swamp deposits. Extensive soil development in the upper portion of the succession is inferred from the thick unlaminated ironstone nodule-bearing fine-grained sediments. This also indicates the stability of the fluvial channels.

284

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Laminated siltstone

S andstone

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PJ^IJ Coai

\_f_f\ Sbaiy coal

Facies symbols (abreviations) are from Miall (1985)

m

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•'.'''// Ocws-boddins

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^ Plant fragment

Fm

Fm

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floocrpMn

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floobpisin

Fig. 3.24

Measured sections showing multistorey channel sandstones in MS-8 (a) and floodplain and crevasse splay deposits in MS-5 (b).

287

sw NE Middle seam

10 T

5 10 15 20 mtjtrsjsj

S\sfa i,ngg« W " '

Scale in metres

Fig. 3.25

Schematic facies relationships on the northern side of Hatari Pit (1990) (A) and Siera Teggo River, near Power Rig Borehole No. R840 (B).

(A) Two channel sand bodies stacked in fine-grained strata. Channel 1 shows erosional surface above mudstone and coal seam with lag deposits and lateral accretion to the southwest. Planar cross-beds are observed in the lower part of the channel sand. Channel 2 shows a narrower channel (probably part of the main channel). A n erosional surface and lag deposits are found above the mudstone and coal seam. Cross-beds and plannar bedding occur in the lower part of the channel sand.

(B) A crevasse splay cross-bedded sandstone deposit above floodplain silty mudstone association. Initial tilting and sharp erosional contact between the sandstone unit and the underlying sediments indicates a proximal splay deposit. Increase of grain size upslope to the top of the strata indicates progradation of the splay to the right (main channel

w a s on the left).

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292

EXPLANATION

A - Planar cross-beds in janditono B = Planar cross-beds tn sandstone C = Planar cross-beds in sandstone D = Planar cross-beds In sandstone E = Planar cross-beds in sandstone F = Logs at the base oTtfae Sangatta G = Planar cross-beds in sandstone H = Cross-Jjunmations in silty

above the Middle seam (CN-1). below the Sangatta seam (HT-9). above the Sangatta seam (HT-2). above the Sangatte seam (HT-7). above the Sangatta seam (HT-3). seam (HT-Ht). above the Pinang seam (ROM-1).

above the Pinang seam (EW-7).

96000

20000Q

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192000

99000 102000

Fig. 3.30 Palaeocurrent directions from clastic sediment seams, Sangatta Coalfield. m e n C associated with the coal

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Fig. 3.33

a) showing typical composition of sandstone above the Sangatta coal seam. Note the significant porosity in the sandstone. Sample (No. HT-3A) was taken from Hatari Pit, Sangatta Coalfield. Field Width of photo (FW) = 3.7 m m .

b) showing the crossed-nicol view of sandstone sample as Fig. 3.33a.

C) showing significant amount of volcanic rock fragments (V) in sandstone sample CN-B (C-North Pit, Sangatta Coalfield) above the Middle seam. Note the presence of plagioclase (P) in the sandstone. F W = 3.7 m m .

d) showing the crossed-nicol view of sandstone sample as Fig. 3.33C.

e) showing significant amount of chert (CH) and rock fragments (RF) in sandstone sample HT-3B (near the base of channel sandstone D, above the Sangatta seam, Hatari Pit, Sangatta Coalfield). Note the large proportion of porosity (PR) in the sandstone. F W = 3.7 m m .

f) showing the crossed-nicol view of sandstone sample as Fig. 3.33e.

g) showing coal components in sandstone sample HT-2 (channel sandstone D, above the Sangatta seam, Hatari Pit, Sangatta Coalfield). Note the more compactability/ductihty of the coal components (C) during diagenesis and quartz inclusions (QI) trapped within the coal. Photo was taken with parallel nicol in transmitted light microscope. F W = 3.7 mm.

fr> showing more compactability of coal component associated in sandstone (HT-2, channel sandstone D, Hatari Pit, Sangatta Coalfield). Note the bending characteristic of coal maceral (C) affected by sandstone compaction during diagenesis. Photo was taken from MPV2-Leitz reflected light microscope. F W = 0.355 m m .

Fie. 3.33

297

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FIGURES TO CHAPTER 4

298

C3004 gamma ray log density log

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1 clean coal

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Fig. 4.1a G a m m a ray and density logs used in identifying vertical and lateral variations of coal benches, dirt bands and clastic interseam strata in the Sangatta Coalfield.

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Fig. 4.9 Three models o n vertical variation of sulphur contents in the Sangatta coal seam, Sangatta Coalfield.

308

Air dried sulphur content (*/•) p p p a p a

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Fig. 4.10 Typical vertical variation of sulphur contents in low sulphur coals from the Sangatta seam Note, mostly the sulphur content is consistently less than 1 % from the top to the bottom of the seam, and the variations are not dependent on ash yield. Heavy line = sulphur content, dash line = ash yield

309

Air dried sulphur content (%)

Fig. 4.11 Typical vertical variation of sulphur contents in moderately high sulphur coals from the Sangatta seam. Note, elevated sulphur contents are mostly in the uppermost part of the coal seam.

Air dried sulphur content (%) ) — to <HJ -h. <Ji CN -J

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311

Caiorific value (cal/gr, daf) CUlorific value (cai/gr, daf)

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Volatile matter (%, daf)

Fig. 4.13 Typical vertical variation of volatile matter content and calorific values in the Sangatta seam. Heavy line = volatile matter content, dash line = calorific values.

FIGURES TO CHAPTER 5

312

120 GEE LAP

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Fig. 5.1 Procedure of coal sample preparation for petrographic analysis (modified from Hutton, 1984).

313

POLISHED BLOCKS i

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AIR OBJECTIVE EXAMINATION

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Fig. 5.2 Procedure in etching coal samples for detailed vitrinite analysis.

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317

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318

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Fig. 5.7 Dendogram from cluster analysis of petrographic data from the Sangatta seam (abbreviations explained in table 5.2).

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Fig. 5.14 Lithotype profile of the Sangatta seam in Drill hole F5304.

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Rank

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Vol. M. d. a. f.

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Applicability of Different Rank Parameters

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Fig. 5.17 Plot of the Sangatta coal rank levels in Teichmuller and Teichmuller's

coalification diagram. Rank levels: Rvlii = coal rank based on dried ash free volatile

matter; R ^ = coal rank based on vitrinite reflectance; and P^-y = coal rank based

on moist mineral matter free calorific values.

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Fig. 5.19 Plots of the Sangatta petrographic data on Diessel's TPI-GI diagram.

331

EXPLANATION

W o o d y tissue (angiosperm) derived vitrinite

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B: Transverse section

Degraded tissue derived vitrinite (detrovitrinite)

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Fig. 5.21 Schematic presentation for the distribution of inferred precursor plants of vitrinite macerals in the Sangatta coal seam, Sangatta Coalfield.

333

PLATE 5.1

a).Telocollinite band (T) in detrovitrinite groundmass (D) from the Sangatta coal, number 24812. Rvmax= 0.68%, field width = 355 um, reflected light mode.

b).Telocollinite band (T) with well preserved suberinite (S) from the Sangatta coal, number 24747. Rvmax= 0.67%, field width=225 um, reflected light mode.

c).Eu-ulminite with corpogelinitic cell filling (F), from the Sangatta coal, number 24732. R vmax = 0.69%, field width = 410 |im, reflected light mode.

d).Eu-ulminite with porigelinite cell filling (F) and carbonate in cracks (C), from the Sangatta coal, number 24733. Rvmax = 0.66%, field width = 410 um, reflected light mode.

e).A pair of cutinite (C) laminae associated with leaf resinite (R) and phyllovitrinite (V), from the Sangatta coal, number 24744. Rvmax = 0.65%, field width = 460 um, reflected light mode.

f) .Detrovitrinite (D) with huminitic fragments, sclerotinite (Sc), sporinite (Sp) and liptodetrinite, from the Sangatta coal, number 24750., Rvmax = 0.61%, field width = 255 um, reflected light mode.

g) .Detrital resinous bodies (R) in detrovitrinite (D) associated with sclerotinite (Sc) and liptodetrinite, from the Sangatta coal, number 23857. Rvmax = 0.68%, field width = 410 [im, reflected light mode.

h).Cell lumens of semifusinite (S) filled by detrovitrinite (D), Sangatta coal, number 24747. Rvmax = 0.66%. Field width = 285 um.

Note: All samples are particulate blocks and were examined under immersion oil.

PLATE 5.1

335

P L A T E 5.2

a).Desmocollinite (D) with suberinite (S) from the Sangatta coal, number 25064, Rvmax = 0.60%, field width = 455 um, reflected light mode.

b).Corpogelinite (C) and porigelinite (P) as cell lumen filling in eu-ulminite, from the Sangatta coal, number 24750, Rvmax = 0.61%, field width = 565 um, reflected light mode. Note the two different orientations of the cells.

c).Gelovitrinite (G) in suberinised cell walls, from the Sangatta coal, number 23857, R vmax =0.68%, field width = 410 um, reflected light mode.

d).Similar occurrences of resinite (R), corpogelinite (C) and porigelinite as cell lumen infillings, from the Sangatta coal, number 24744, Rvmax =0.65%, field width = 230 um, fluorescence mode. Note the change of fluorescence intensity from the resinite to the corpogelinite.

e).Same field as d) but in reflected light mode.

f).Well preserved cutinite (C) indicating morphology of a leaf with phyllovitrinite (V), from the Sangatta coal, number 24812, Rvmax =0.68%, field width = 355 um, reflected light mode. Note the association desmocollinite (D) surrounding the cutinite.

g).A pair of cutinite (C), from the Sangatta coal, number 25055, R vmax =0.60%, field width = 230 um, fluorescence mode. Note the different thickness of the cutinite.

h).As g), in reflected light mode. Note the associated phyllovitrinite (V) included within the cutinite.

Note: All samples are particulate blocks and were examined under immersion oil.

PLATE 5.2

33

PLATE 5.3

a).Well preserved thin suberinised cell walls (S), from the Sangatta coal, number 24751, R vmax = 0.68%, field width = 355 um, fluorescence mode.

b).As a) but in reflected light mode. Note the gelovitrinite (G) in the suberinised cells.

c).Thick suberinite (S) partly broken, from the Sangatta coal, number 24746, Rvmax =0.67%, field width = 355 um, fluorescence mode.

d).As c) but in reflected light mode. Note the associated detrovitrinite (D) between the broken parts of suberinite.

e).Partial fusinised resinite or micrinite (M) associated with detrovitrinite (D), from the Sangatta coal, number 24734, Rvmax =0.63%, field width = 285 um, reflected light mode.

O.Resinite (R), from the Sangatta coal, number 24815, Rvmax =0.67%, field width = 355 um, reflected light mode. Note the increase in intensity of vitrinitic material toward the top.

g).Semifusinite (S) in detrovitrinite groundmass (D), from the Sangatta coal, number 25062, R vmax =0.60%, field width = 355 um, reflected light mode. Note the mineral fillings and empty cell lumens and the sharp contact with the associated detrovitrinite.

h).In-situ inclusions of sclerotinite (SC) in telovitrinite (T), from the Sangatta coal, number 24737, R vmax =0.70%, field width = 410 um, reflected light mode.

Note: All samples are particulate blocks and were examined under immersion oil.

PLATE 5.3

339

P L A T E 5.4

a).Clay mineral (C) associated with detrovitrinite (D), from the Sangatta coal, number 24728, Rvmax =0.65%, field width = 230 um, reflected light mode. Note the detrital nature of the detrovitrinite.

b).Clay mineral (C) associated with telovitrinite (T) originated, from the Sangatta coal, number 25062, R vmax =0.60%, field width = 355 um, reflected light mode. Note the pair of thin suberinite layers associated with the telovitrinite.

c).Carbonate inclusion (C) in detrovitrinite (D), from the Sangatta coal, number 23854, Rvmax =0.69%, field width = 640 um, reflected light mode. Note the less compactable nature of the carbonate.

d).Carbonate veins (C) in cracks developed in telovitrinite (T), from the Sangatta coal, number 24818, Rvmax =0.63%, field width = 355 um, reflected light mode. Note the faint fibrous appearance of the carbonate perpendicular to the veins.

e).Carbonate veins (C) associated with pyrite (P) in cracks developed in vitrinite, from the Sangatta coal, number 24748, Rvmax =0.68%, field width = 355 um, reflected light mode.

f).Framboidal pyrite (P) associated with clay mineral (C), detrovitrinite (D) and sclerotinite (Sc), from the Sangatta coal, number 24735, R vmax =0.60%, field width = 265, reflected light mode. Note the orientation of the pyrite and sclerotinite controlled with bedding direction.

g).Cracks (C) are well developed only in telovitrinite (T), from the Sangatta coal, number 24744, Rvmax =0.65%, field width = 460 um, reflected light mode.

h).Framboidal pyrite included in vitrinite, Sangatta coal, number 25011. R vmax = 0.51%. Field width = 410 um.

Note: All samples are particulate blocks and were examined under immersion oil.

PLATE 5.4

341

P L A T E 5.5 (from etched samples)

a).Telinite (T) showing thin fibre tracheids cells with multiseriate rays (R) formed by gelified materials (corpogelinite), from the Sangatta coal, number 24744, field width = 455 um, reflected light mode (oil). Tangential section.

b).Telinite (T) showing thick/dense tracheid cells with parenchyma rays (R), from the Sangatta coal, number 24737, field width = 285 um, reflected light mode. Note the absence of vessel elements in this woody derived vitrinite. Cross-section.

c).Degratelinite (D) showing partial degraded tissues, from the Sangatta coal, number 24733, field width = 285 um, reflected light mode.

d).Detrotelinite (D) showing well oriented vitrinitic fragments, from the Sangatta coal, number 24740, field width = 355 um, reflected light mode. Note the homogenous fragments of vitrinitic materials in the detrotelinite.

e).Vitrodetrinite (V) showing intensive physical fragmentation/ degradation and chemical gelification, from the Sangatta coal, number 24734, field width = 285 u m , reflected light mode. Note the heterogenous fragments of the vitrodetrinite.

f).Resistant corpogelinite (C) in moderately gelified vitrinitic material (V), from the Sangatta coal, number 24734, field width = 225 um, reflected light mode. Note the birefringence of the gelified material. Left = unetched; right = etched

g).Cork tissue (C) with periderm and woody tissue (W) in the inner side, from the Sangatta coal, number 24733, field width = 355 um, reflected light mode. Top-left = unetched; right = etched

h).Well preserved tissue (T) associated with vitrodetrinite (V), from the Sangatta coal, number 24740, field width = 355 um, reflected light mode.

Note: All are from etched samples and in immersion oil.

PLATE 5.5

'•:v, j * * ^ • J. ^> V N

343

P L A T E 5.6 (botanical structures in the Sangatta coal and modern plants)

a).Tangential section of telinite derived from angiosperm wood showing tracheid cell walls (T) and multiseriate rays (R) formed by gelified materials (corpogelinite). Reflected light in oil immersion mode. Number : 24750. Field width = 355 um.

b).Tangential section of telinite derived from angiosperm wood showing tracheid cell walls (T) and multiseriate rays (R) formed by gelified materials (corpogelinite). reflected light in air objective mode. Number: 24750. Field width = 900 um.

c).Cross-section of telinite derived from angiosperm wood showing tracheid cells (T), parenchyma rays (R), and vessel element occupied by corpogelinite (C). reflected light in air objective mode. Number: 23844. Field width = 700 um.

d).Cross-section of vitrinite derived from cork tissue showing an absence of woody structure, reflected light in air objective mode. Number 23847. Field width = 900 um.

e).Tangential section of woody tissue from Dyera spp. (dicotyledonous angiosperm) showing fibre tracheid cells (T) and multiseriate rays (R). reflected light in air objective mode. Field width = 1150 um. Comparable with a and b.

f) .Cross-section of pandanus tissue with vessel elements but without woody structures. reflected light in air objective mode. Field width = 1 1 5 0 um. This type of plant tissue was hardly observed in the Sangatta coal (probably due to the lack of preservation).

g).Cross-section of woody tissue from Gonystylus spp. (dicotyledonous of angiosperm) showing fibre tracheid cells (T), parenchyma rays (R) and vessel elements (V). reflected light in air objective mode. Field width = 1150 um. Comparable with c.

h) .Cross section of cork tissue from Calophyllum spp. (dicotyledonous angiosperm) showing gelified materials included in suberinised cell walls and no woody structures in this outer part of the plant, reflected light in air objective mode. Field width = 565 um. Comparable with d.

Note: A, b, c, and d are from the Sangatta coal samples and e, f, g, and h are from modern plants of Sarawak, Borneo (Kalimantan), Malaysia (modern plant blocks supplied by Dr J S Esterle).

PLATE 5.6

FIGURES TO CHAPTER 6

345

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Regression Results:

i Pairs : 161

Slope : Intercept . Correl. coeff.:

.103 i.472 .328

25. 38.

ftshply

Fig. 6.19 Correlation of ash yield & o m ply samples (ashply) and ash yield from composite samples (ashcom), Sangatta seam. Ash yield values are in percent.

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Fig. 6.21 First order trend surface map (a) and the residual map (b) of ash yield from ply samples, Sangatta seam Contour values are in percent.

95000 197000

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367

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96000

aswscoe.plt

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thickness.

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6.563 3.8247

8. 400. 889. 1288. 1608. 2888,

Distance

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Par

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Pairs

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asliuin.pcf

1131

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ininun: tiaxinun:

san : War. :

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6,563 3.0247

488. 888. 1288. 1600. 2888. 2488,

Distance

Fig. 6.26 Four directional variograms of the smoothed ash yield data from ply samples, Sangatta seam, indicating the most continuous ash yield distribution toward N N E (80). Note: In the variogram computation, 0° = E-W , 45° = NE, 90° = N-S.

372

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r

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Sulply

1.2

Regression Results:

8 Pairs : 156

Slope .' Intercept .' Correl. coeff..

.839

.858

.935

1.6

Fig. 6.28 A high correlation between sulphur content from ply samples (sulply) and sulphur content from composite samples (sulcom), Sangatta seam.

374

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196000

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96000 97000 98000 99000

95000

94000

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196000

195000

i-l 194000 95000 96000 97000 98000 99000 100000

Fig. 6.30 First order trend surface map (a) and the residual map (b) of sulphur content. Contour values are in percent.

95000 197000

196000

195000

194000 95000

95000 197000

196000 -

195000 -

194000 95000

96000

376 4TH TREND SURFACE OF SULPHUR (STREND4.PLT)

97000 98000 99000 100000 19701'

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4TH TREND SURFACE RESIDUAL OF SULPHUR (SULRES4.PLT)

96000 97000 98000 99000

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96000 97000 98000 99000 '—I 19400C 100000 '

Fig. 6.31 Forth order trend surface map (a) and the residual map (b) of sulphur content. Contour values are in percsnt.

95000 97000

196000 -

195000

194000 95000

95OO0 197000

196000

195000

194000 95000

377

MOVING AVERAGE OF SULPHUR (SULMOV.PLT)

96000 97000 98000 99000 100000 197000

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96000 97000 98000 99000

= 196000

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194000 100000

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196000

195000

194000 96000 97000 98000 99000 100000

Fig. 6.32 Moving average map (a) and coefficient of variation map of sulphur content (b), showing an increase of the values toward the southwest and increase the variability to the central zone. Contour values are in percent for (a).

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HistcgraH

Data file: vn-cv.Jat S t a t i s t i c s

N Total N Hiss N Used

Mean Variance Std. Dey

Skewness Kurtosis

Hininun 25th V, Median 75th V,

mum

147 8

147

5.221 .384 .618

11.863 .788

2.848

4.886 4.758 5.040

7.108

noistura

Fig. 6.35 Histogram and statistical parameters of moisture content data, Sangatta seam.

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distance (m)

Fig. 6.38 Omnidirectional variogram (a) and directional variogram (b) of moisture content data, showing a long range, nugget effect, a slope anisotropy. The gentlest slope is toward

O20° and the steepest slope is along the 110°direction.

384

48.

3B.-

29.

18.

8, 13888.

Histogr-an

Data file: vn-cv.dat

13489.

Calorific (value)

13888.

S t a t i s t i c s

H Total N Hiss NUsed

Hean Variance Std. Dev '/, cu, Skewness Kurtosis

Hininun 25th 'A Hedian (bus /.

Maximum

147 8

146

13516.528 32183.158

178.387 1 r\im

l.Xt - 1K

. 1-JU L.(JU

13825.588 Lwfo.loo

iOjJi.OOD

lb'bZb.288

Fig. 6.39 Histogram of calorific vdue data, Sangatta seam. The values are in BTU/lb.

cd 4-4

a 73 CO

>

S-H

O

13 o C+H

o

o-ccj

S 0)

2 >

p IP * <U . . »Vr

Id «1 W CO

Co 1—t

s U U> iH

3 P O O 4-> *->

o o

UU o

386

CL CN Q Z UJ

cc

CL

Q

UJ CC

387

Fig. 6.42 Omnidirectional variogram (a) and directional variogram (b) of calorific value data.

388

Histogram

Data file! vn-cv.dat S t a t i s t i c s

H Total H Hiss H Used

Hean Variance Std. Bey zC.V. Skeaness Kurtosis

limnun 25th 7. H i •

etiian

75th* Haxinun

147 8

147

43.841 1.858 1.829 2.347 -.838 4.523

38.722 43.178 43.736 dd C£.7 l i . yJU I

46.858

Uol-atila H (after)

Fig. 6.43 Histogram of volatile matter content data (% in dry ash free basis).

s o H-> G O U 4-4

c aj 4->

c o o U <U ts rt g ej

« <*}

o > <+-4

o /—V

e OH C3

g 1> WJ ca u. (!) > a W1

1 <j

e *o c ea /^s etf S ^

CH ra g S3 n C o U Tf "* C &D to

c/> .—r CQ « X u y * -c W) CQ

& *c s_ 4-4

u. u (1 u, <u &

pc s fe 09 U 3 ?3

>

390

CN

O >

"D C OJ

o >

J) "H—

CQ

"o > o

a ca g u CJ

3 «3

•o «J

rH

•n u O

C O o CJ w

C ca /—\ <a N—/

ca g 4) CJ

3 01 T3 C CJ •C

u CJ •O u O 50 Ui • rH

to <«n • *

O

«>b to

09 09 CQ .fi

rC cn ca

s u (J CJ OH

c p Is cfl

3 ca > u 3 a H-H

c c U

c 1) H—

c o '-> CJ

ca g

391

2.50 T

2.00--

g 1.50 4

E

I 1.00 +

0.50 --

a

0.00

0.00 + -t-

500.00 1000.00 1500.00 2000.00 2500.00 3000.00 3500.00 4000.00 4500.00

distance (m)

0.00 •+- -t-0.00 500.00 1000.00 1500.00 2000.00 2500.00 3000.00 3500.00 4000.00 4500.00

distance (m)

Fig. 6.46 Omnidirectional variogram (a) and directional variogr.am (b) of volatile matter content.

392

94000 200000

199000 -

198000

197000 -

196000 -

195000 -

194000 94000

95000

delta volatile matter (dvol.plt)

96000 97000 98000 99000 100000 200000

199000

- 198000

- 197000

- 196000

- 195000

95000 96000 97000 98000 99000 194000

100000

Fig. 6.47 Delta volatile matter content map.

393

0.0111 0.1760 0.3409 0.5058 0.6707 0.8356

-0.0714 0.0935 0.2584 0.4233 0.5882 0.7531 0.9180

r T T T T 1 Si02 0.7106

— K20 0.5009

— AL203 0.6625

— Ti02 0.0603

— P205 -0.0347

— Fe203 0.4580

— Mn304 0.1646

— S 0.7318

— ORGS 0.2310

— PY 0.3788

— SUL 0.0274

— Na20 0.1008

C

H

N

— CaO

— MgO

— S03

— C02

— ASH

O

0.7380

0.2977

-0.0199

0.8350

0.8814

0.6350

0.2395

0.1556

-0.0714

DENDROGRAM - VALUES ALONG X-AXIS ARE SIMILARITIES

Notes: ORGS = Organic Sulphur PY = Pyritic Sulphur SUL = Sulphate Sulphur ASH = Ash yield

Fig. 6.48 Dendogram of ash composition and ultimate analytical data, Sangatta seam.

394 o o o

oo 0^4

0 0 0

01

*~

o a a

o o o

o • *

01 o

-o o o o

u

O

CJ > •c CJ T3 r-H 03 Ui a a g >> a b

ca <!> •4—

ea CJ

'02

<« 0

JO W

9-ca f= 0

en C5 Ui «J

5a eo c > b g •0 c ca 'c?

& l

ca g u 3 O £ O u o> •* VO

+-4

c u f 1

u

c n

CJ u. ca DO

u rH; _I5 f3 > Ui P O c 0 U •

ca 00

ca 00 s ca &0 u ,fi H—

.fi 03 ca ca O CJ G •** 00 H— C

F. « *«

60 -HJ-H

to

395

95000 197000

96000

clay 1 .pit

97000 98000 99000

196000

195000 -

194000 95000

a

95000 197000

100000 197000

- 196000

195000

96000

96000

97000 98000

clay2.plt

97000 98000

99000

99000

194000

196000 -*

195000 -

194000

100000

100000 197000

196000

195000

98000 99000 100000 194000

Fig. 6.50 First order trend surface map (a) and second order trend surface map (b) of silicate and clay mineral-derived elements in coal ash, the Sangatta seam. Contour values are in percent.

o o o o

oo

!r

o o o

o o o

CL

< 00

eg o

o o CO

cn o - o _ o o o

o o o 00 Oi

o o o 01

o o

ca g ca eo c ca CO <u r£H <rH

o x: Vi ca ^^ ca O CJ

2

co <H-

o

ca

o>S a o R

o o a

o o CO r*

o o o <o

o o o tfl

o o o

go o •H-Ol

CJ

eo

2

I eo c

'1 g •a e ca

ca

g in r»*

B a o U

g r-4 «

eb to

397

aj .c 4-1

C •*H

a c OJ g ci) l-H

<u T3 OJ > •c OJ "O CI) cd xi Cu V) O fi Cu •o r ca n> •4-4

cd Xi O. fi c/) •>

HSJ ca c o •§ f)

4-1

o c o 4-4

cd

c Xi g o U <N in VO

e>b to

. 4—>

C OJ r» u, «u Oi

c 'rH

Ul 3 n 4->

c O CJ

fi cn crt

cd O o cd 4—4

cd

CO

398

o_

o

a. o o CL

<

o

xs Vi cd

73 o CJ

C 4-J

c o CJ w 4-4

O £ o c el D H " cd as

g g «^> Ui ^

15 ^ ca B

g I •§8 cd <d /-N Si ed «d s-' ao

&§ " rJ! u, <U

C g o o cn vd eb to

399

OL

<

o

Cn

cn

+ a O

cd O

o

c fl) 4-4

c o o O OO

? o cd u Xi

OH cd

g n) Oil rrt Ui

fl) > cd 00

c > n F, T3 C cd

Id OH cd

g UH

fi O 4—> fi

n U

f m vO

ob • rH

to

4-1

c y Cr

c ^H

1 c/1

eu 3 cd

> u. 3 O

c o U , g cd OJ 1/9

3 4—4 cd oo c cd CO a) .3 •4^

g o 4-4

xi Vi cd

400

95000 200000

199000

198000 -

197000

196000 -

195000 -

194000 95000

96OO0

NITRO.PLT 97000 98000 99000 100000

200000

- 199000

- 198000

- 197000

- 196000

- 195000

194O00 96000 97000 98000 99000 100000

Fig. 6.55 M a p of nitrogen content obtained from ultimate analysis, Sangatta seam. Contour values are in percent.

401

Statistical Summary

Number oF Pairrts 80

Excluded Pointa 18

Covariance 0.080

Correlation Coefficient ... 0.897

SULPHUR (%

Fig. 6.56 Correlation between total sulphur and organic sulphur for the Sangatta coal seam.

402

95000 200000

199000 -

198000 -

197000

196000 -

195000 -

194000

RATIO (ORG->NON.PLT)

96000 97000 99000 100000 200000

- 199000

- 198000

- 197000

- 196000

- 195000

95000 96000 970O0 98000 99000 ~ 100000 194000

Fig. 6.57 M a p of organic/inorganic sulphur ratio in the Sangatta seam.

403

EXPLANATION

1 -Statistical population

2 - Variogram

3 -Isotropy of directional variograms

X -Average thickness

CV -Coefficient of variation

R - Fit of trend surface

WESTERN ZONE 3

.X = 6.9 W CV = 0.39 R = 0.77

200000

CENTRAL ZONE

3

EASTER ZONE

X = 6.2 M CV = 0.41 J* = 0.37

X = 5.2 M CV = 0.53 R = 0.23

- 198000

196000

95000 194000

97000 99000

Fig. 6.58 Statistical summary of the thickness data of the Sangatta seam in the four geological zones.

404

EXPLANATION

A Statistical distribution of sulphur content

Vertical variation of sulphur content from ply samples x K

r y

CO 0)

A x e s of major and minor ranges

of sulphur variogram

WESTERN

200000

- 198000

196000

J 194000 95000 9700Q 99000

Fig. 6.59 Variations in statistical population .and vertical development of sulphur content in the Sangatta seam, Sangatta Coalfield.

FIGURES TO CHAPTER 7

405

N

t 200 000

198000

196000

95000 9700Q 99000 194000

Fig. 7.1 Distribution of the Sangatta coal seam and the four spatial zones, Sangatta Coalfield. Locations of an extensive channel sandstone (1) and a major washout zone (2) are indicated on the map.

406

LOW SINUOSITY CHANNEL SAND

RIBBON SAND BODY

APPROXIMATE m BURNT ASH

AFTER PEAT FIRE

Fig. 7.2 Hypothetical model for the development of the Okavango River, Bostwana Africa, showing a confinement of the channel by levee vegetation and peat deposit in the latter

stage (after Stanistreet et al, 1993).

407

vi

*o

g e Vi

u cu

I CO

u

OJ

C

o In

C

'I o C3 I-I

o o CQ

408

409

410

CM

"3 •o

o 5

0) •o

o 5

411

Bukit Asam Sangatta

Om

• e eg

u o ©

ta

E w O

u. c UJ

ra 3

<ZDO •—,

Om ~

100

A.1 Seam

A2 Ser.m

B Seam

200

C Seam

o c o u o

c 100

o a E w O

u. a a. a a jt

15 CD

P3 Seam

P2 Seam

P1 Seam

Pinang Seam

Middle Seam

200 — i —

Sangatta Seam

B2 Seam

Fig. 7.7 Comparison between geological conditions in the Bukit Asam Coalfield (South Sumatra Basin) and the Sangatta Coalfield (Kutei Basin).

412

TYPE OF BASIN

STATISTICAL POPULATION

FOR THICKNESS

THICKNESS (AVERAGE)

COEFFICIENT OF VARIATION

RANGE OF VARIOGRAM

SILIMUGGET RATIO

THICKNESS DISTRIBUTION (FROM DIRECTIONAL VARIOGRAMS)

FIT OF TREND SURFACE

SPATIAL VARIABILITY (FROM MOVING WINDOWS STATISTICS)

THICKNESS AND VARIABILITY CORRELATION

SANGATTA SEAM (KUTEI BASIN)

Continental margin or back arc basin

BIMODAL NORMAL

thickness (m)

5.8 METRES

0.47

420 METRES

o OT iom is» am an distance (m)

Al SEAM BUKIT ASAM (SOUTH SUMATRA BASIN)

WsU defined back arc basin

UNIMODAL NORMAL

thickness (tn)

6.8 METRES

0.33

1000 METRES

1.9

ANISOTROPY AND ZONING

R = 0.10 (first order) = 0.38 (second order)

HIGH

NEGATIVELY CORRELATED

7

6-

2 Si

a «.

=41 2J

0 C

A r

~/T i

as ian is! am distance (m)

23E

2.9

ISOTROPY

R = 0.45 (first order) = 0.50 (second order)

LOW

.2 mr

« > *1 a — w -

o (J ,

" • 4 1 . |

thickness (m)

i

i

•

• •

NO CORRELATION

Fig. 7.8 Statistical summary of the thickness data from the Sangatta seam (Kutei Basin) and

Bukit Asam Al seam (South Sumatra Basin).

413

S A N G A T T A S E A M

1. Sedimentary facies changed

locally

2. Overbank sed. partings

3. Tapering, washouts, splitting

4. Common syn-dep. deformations

a). Less mature sed. setting

b). Less stable peat -forming platform

c). Unstable basin

Al SEAM

Sedimentary facies changed over a long distance

Lack of overbank sed. partings

Lack of tapering, washout and splitting

Lack of syn-dep. deformations

More mature sed. setting

More stable peat-forming platform

More stable basin

Fig. 7.9 Comparison of the geological conditions and interpreted peat development systems between the Sangatta and Al seams.

414

:0NirEROU8, BROAO-LEAVED ANO RIPARIAN PLANTS

SHRUBBY ANO HERBACEOUS PLANTS. FERNS. ALQAE. AND SPHAGNUM

CONIFEROUS. 8R0AC ANO RIPARIAN

WOOD PEAT (HUMINITE-RICH COAL)

Fig. 7.10 Raised bog model for the thick coal scams in the Powder River Basin (U.S.A),

showing spatial variation in peat and vegetation types (after Flores, 1993).

^/Cy.r^yff^M,, water labia

T ? 5 T y

H D 0

WELL PRESERVED W O O D >85X V

MIXED MATERIAL .x 65-84S V

POORLY PRESERVED SHRUBS < 6 S S V

FIRECLAY

SANDSTONE

Fig 7 11 Hypothetical model for the lower bench of the Upper Hence seam, Kentucky (U.S.A), showing a raised mire with spatial variation of peat and vegetation types (after Esterle

and Ferm, 1986).

FIGURES TO CHAPTER 8

415

CO HI o or. 3 O CO UJ

Q LU

LU

> o o CO

Q Z 3

CO LU

O E 3 O CO LU c Q LU

r-

z LU a —

UJ

a z < c

LU

> r-

<

5 y LU C to

h- -

— o — ffl < CD O = 0.

—1

< u 1— _ •

r-O

> •

c

= !— Z

#• *

UJ r— < cr r-z o 2 u

o L-r-

< o " •

z

2 LJ r-

5 < LU

2

L. Z > o r- P < CJ - 3

5 O - e CJ 0.

1"

+ +

- V.

i ; = = ;_ U.

z — — c

w u. > i_

LU

c

a 2 O Z c u LU

r U K ~" < L_

- z > = s = U = K z < L-= 2 =

> c l_ L_

U

< z c c < 2

>

- 2 < 2

z o c « = o < CJ 2 ^

c — w

£ 2 L_ LU C CJ C Z c = o = - w C ; u B — z c

«

w

2 w

c S

§ 5 c 5 z' « = LU

- c V)

C 2 C Z c CJ L_

e w

CO

< E — r-

< 2 < Z C > z o u z c z c: z

416

Demonstrated coal resources

Total in situ coal

Disposition suitable for mining

Quality suitable for use

Original in situ coal reserves

Remaining in situ

coalr jserves

Inferred and undiscovered coal resources

^ Disposition unsuitable

for mining (e.g. too deep, too thin)

Quality unsuitable for use

(e.g. excessive ash or sulphur)

Not available for mining or previously mined-out

z: Suitable for surface mining

SC

Suitable for underground mining

Remaining recoverable coai

reserves

__ Anticipated losses in mining operations

Remaining marketable coal reserves

Discarded as refuse in coal preparation

Fig. 8.2 Characterisation of coal resources from in-situ coal to marketable reserves (from Ward, 1984).

417

• Ease of mining Coal recovery •

or Mining costs

Fig. 8.3 Coal reserves distinguished from three main factors; geological, minability and marketability (from Ward, 1984).

418

CO UJ >

os UJ

3 OS

g CO

Z UJ _J 03

UJ

(5

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very

factor

App

mini

reco

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CO UJ U OS

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00

TABLES

TABLES TO CHAPTER 2

419

INDONESIAN

LETTER CLASSIFICATION

UJ

CJ

CE

UJ TZ

cr

UI CJ CE I—

cn _j CE CJ

o _]

c

C c <v +-

o

C3

4i

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m TO C n ex £ D

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17

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CQ

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£

0-

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1T>

1—

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c

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CV

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c

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LO

C •r-l

w r; CJ

S TD C cd l-H OJ

E ctj

6 o u

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cu

cd r-

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CQ

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CU r—-•

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420

Stratigraphy of

Le u p o 1 d and Van

der Vlerk ( 1931 )

KRMPUNG BRRU

BEDS

(Tgh)

UPPER BRLIKPRPRN BEDS <Tf3)

LOWER BRLIKPRPRN

(BEDS)

<Tf2>

PULU BRLRNG

BEDS

(Tf 1 )

BEBULU BEDS

(Te4~5)

PEMRLURN BEDS (Tel-3)

R

S y S t «

e V i S

m

PI 1 o c e n e

U p p e r

M i o c e n e

M i d d l e

M i o c e n e

c M V O

E

L t>

I 0 _l

*-a -I

-A

L a LU

U p p e r

0 1 i g o c e n e

e d S t r a t i g r a p h y ( t h i s p a p e r )

B l o w

Z o n e

N19

N18

N17

N16

N15

NS TO N14

N8

N7

N6

N5

N4

F o r m a t i o n

. r

KRMBOJfi

FORMATION

PRRNGRT FORMATION

u n c o n f o r m i t y

LOR KULU FORMATION

LOR DURI

FORMATION

B a t u p u t i h L i m e s t o n e

* Th » age o{ th* top gi

P r a n j a t F o r m a t i o n Is

Thick n»ss <»>

470

137E

800

450

2-50

E n V i r or>-m e n t

R l l u v i a 1

f l o o d p l a i n

R 1 1 u v i a 1

f 1o o d p l a i n

D e l t a i c to

m a r i n e

S h e If

D e e p

m a r i n e

•id b o t t o m of th«

u n c e r t a i n

Table 2.2 Stratigraphy of the Mahakam Coalfield, central Kutei Basin (from Land and Jones, 1987).

TABLES TO CHAPTER 3

421

COMPONENTS

Monocrystaline quartz

Polycrystaline quartz

Overgrowth quartz

K-felspar

Plagiociase

C h e r t

Radiolarian chert

Vole. Rock Fragments

Met Rock Fragments

Sed. Rock Fragments

Coal Fragments

Tourmaline

Zircon

Chalcedony

Mica

Sericite

Apatite

Opach mineral

Carbonate

Clay mineral .

PORES

HT-6A

40 _

1 tr tr 10

tr

1 1 tr tr tr tr tr 0 0 0 tr 40 0 1

L

HT-3A

50

5 i tr ! tr : 0 ! 10 j

5 ! 5 !

i ;

tr j tr | tr ; tr 1

tr ; o ; 0 i

0 ! tr !

0 | 0 ! 20 i

0 c

HT-3B

30 10 5 tr tr 10 5 5 5 1 1

tr 0

tr 0 tr tr 1 0 5 20

A T I O N S

ITT-6B

30 5 1 tr

tr 10

1 1 1 1 5

tr tr tr 0 tr 0 tr 40 tr 1

CN-A

40 5

1 1

1 10

1 40 1 1 tr tr tr tr

tr tr 0

tr 0 0 1

CN-B

30 5

1 1

1 10 i

t 50 1 tr tr tr

tr 0 0 0 0 tr 0 0 5

20 10

1 tr tr 10

5 5 1 1 40 0

tr 0 0 0 0 tr 0 0 10

a)

MINERALS

Q u a r t z

M i c a

F e l s p a r

A n a t a s e

G y p s u m

K a o l i n i t e

11 l i t e

Montmorilonite

C h l o r i t e

Mixed laver clav

b;

i

A C

c

R

WHOLE ]

n i

': A : C R

i TR i

; R

A C

TR R

ROCK

1 ;

>* * • ^ ;

: A 1

c : R

R ' i

: TR :

!

z u A R TR

TR

TR

E

A TR TR

A

C

A TR TR

TR

L A Y

i

•

A TR TR

TR

v * 1

A TR TR

C

I

z

A TR TR

TR

Table 3.1 Data for petrologjc composition from some sandstone (a) and fine-grained (b) samples in the Sangatta Coalfield.

TABLES TO CHAPTER 5

422

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2920 2922

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3000 3001 3003 3007 3020 3031 3038 3039 3042 3236 3486 3538 3539

3631 3541 3041 3576

EASTING

98360.9 98194.1

99016.6 98714.8 96514.2 96110.6 98380.4

96488.5 96182.4 96615.9 96277.2 96399.9 96966.2 97740.9

97651.8 97391.7 97181.8 97063.4 98823.6 96239.9 98226.9

97655.5 98019.1 98082.4

97513.0 99110.0

NOTES:

NORTHING

195741.6 195519.4 195505.4 195503.2 195987.3 195500.7 195128.3 194598.3 195126.0 195246.0 195457.4 195752.1 195359.6

194775.7 195194.0 194879.5 195127.0 195746.1 195301.4 194822.6 194619.8 194332.5 194863.5 194337.9 195746.9 198455.0

MINIMUM

MAXIMUM

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COEF. VARIATION

TV

28.6 25.1

28.8 23.2 32.8 31.0 16.9 44.6 15.0 30.4

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36.1 20.1 16.2

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15.00 55.30 28.47 9.87 0.35

TL

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7.60 29.90 15.03 5.29 0.35

T V = Total Telovitrinite C O R P = Corpogelinite

DV

60.0 67.4 65.9

67.8 56.6 66.0 68.6 50.2 79.5 63.4

41.6 51.3 60.7 69.9 79.9 62.4 64.2 76.4 66.6 61.6 74.1

75.3 63.9 62.0 63.7 50.0

41.60 79.90 64.19 9.02 0.14

TL = Telinite C O R K = Corkvitrinite D T L = Degratelinite P H Y L = Phylovitrinite

DTR

31.9

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10.00 40.00 25.03 7.40 0.29

D V = Total Detrovitrinite U N D = Undifferentiated vitrinite

VDR

28.1 29.7 40.4

29.8 34.1 43.3 42.1 25.8 53.0 44.9 29.5 32.0 32.6 50.2 48.0 43.6 40.0 40.1 41.5 40.3 52.7 35.3 47.4 49.4

39.8 22.7

22.70 53.00 39.09

8.35 0.21

D T R = Detrotelinite A N G I O = Telinite from Angiosperm wood V D R = Vitrodetrinite

CORP

0.4 0.6 0.2 1.0 0.6 1.7 0.6 1.3 0.0 0.8 1.5 0.9 0.0 0.0 0.0 0.0 0.0 0.6 0.0 0.0 1.0 0.0 0.0 0.0 1.4 1.6

0.00 1.70 0.53 0.58 1.08

CORK

4.5 3.4 3.8 6.5 0.8 0.6 7.4 1.2 0.8 2.5 0.4 0.6 1.8 5.8 2.1 3.5 2.7 0.6 7.2 0.8 6.0 4.6 5.4 5.7 4.3 1.5

0.40 7.40 3.23 2.28 0.71

PHYL

0.8 0.0 0.4 0.0 0.6 0.6 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.8 0.0 0.4 0.6 0.0 0.0 0.0 0.0 0.0 0.4 0.0 0.0 0.0

0.00 0.80 0.16 0.25 1.61

UND

5.3 3.4 1.1 1.0 8.5 1.7 6.1 2.0 4.4 2.5 3.4 2.8 1.3 3.3 1.4 3.6 1.8 2.6 2.5 2.3 2.7 2.6 3.2 4.5 6.5 5.4

1.00 8.50 3.30 1.80 0.55

ANGIO

9.1 2.8 3.9 5.4 18.9 1.5 0.7 25.8 0.2 7.6 20.3 16.7 12.2

0.6 1.4 2.5 1.9 1.3 2.8 9.5 1.6 2.0 2.3 2.3 3.6 10.9

0.20 25.80 6.45 6.90 1.07

Table 5.4 Vitrinite maceral compositions in etched samples from the Sangatta coal seam.

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Data File:

Mean Variance Std. Dev. Coef. Var. Skewness Kurtosis Minimum 25th %tile Median 75th %tile Maximum

Data File:

Mean Variance Std. Dev. Coef. Var. Skewness Kurtosis Minimum 25th %tile Median 75th %tile Maximum

Data File:

Mean Variance Std. Dev. Coef. Var. Skewness Kurtosis Minimum 25th %tile Median 75th %tile Maximum

B A T C H S T A T I OF CLUSTERED DATA FROM SIX

D:\DATA\GR0UP1.DAT

ASH 2.288 .739 .860

37.559 .245

2.463 .800

1.535 2.260 2.970 4.200

VOL. MATTER 40.294

.479

.692 1.717

-1.334 7.039

37.900 39.930 40.360 40.600 41.570

D:\DATA\GROUP2.DAT

ASH 2.049 .653 .808

39.421 .849

3.471 .600

1.493 1.890 2.453 4.400

VOL.MATTER 40.138

.473

.688 1.713

-1.188 8.854

37.100 39.900 40.060 40.435 41.840

D:\DATA\GROUP3.DAT

ASH 2.222 1.922 1.386 62.387

.900 2.976 .500

1.015 1.775 2.990 5.720

VOL. MATTER 39.152 66.178 8.135

20.778 -4.579 22.351

.000 39.945 40.550 41.485 43.100

CAL. VALDE 13618.530 55378.460

235.326 1.728 -.169 3.635

13057.130 13463.940 13633.960 13762.430 14170.130

CAL. VALUE 13615.150 8842.790

94.036 -.691 .923

4.503 13416.880 13549.130 13607.060 13651.530 13935.900

CAL. VALUE 13377.870 16665.920

129.097 .965 .312

4.514 13025.590 13299.500 13377.630 13438.570 13797.610

S T I C S COAL VARIABLES

SULPHUR .648 .068 .261

40.214 1.150 4.659 .200 .550 .570 .685

1.380

SULPHUR .280 .015 .122

43.461 2.956

15.215 .170 .200 .250 .322 .920

SULPHUR .416 .050 .225

54.016 .804

2.662 .150 .220 .390 .550 .970

MOISTURE 4.951 .043 .207

4.175 -.586 2.318 4.520 4.800 5.000 5.108 5.260

MOISTURE 4.795 .074 .271

5.658 .131

3.299 4.100 4.600 4.790 5.000 5.570

MOISTURE 5.787 .304 .552

9.534 .042

2.383 4.670 5.355 5.775 6.200 7.100

THICKNESS 6.968 5.553 2.357

33.818 -.822 4.316 .000

5.403 7.670 8.330

11.110

THICKNESS 6.282 4.064 2.016 32.090 -.183 3.837 .460

5.010 6.570 7.340

11.590

THICKNESS 7.642 3.840 1.960

25.645 .982

3.562 4.600 6.310 6.985 8.880

13.400

stagroup.v6 Table 6.3 Statistical elements for data grouped by

six variable Q-mode cluster analysis.

431

Data File: D:

Mean : Variance : Std. Dev. : Coef. Var. : Skewness : Kurtosis : Minimum : 25th %tile : Median : 75th %tile : Maximum :

Data File: D:

Mean : Variance : Std. Dev. : Coef. Var. : Skewness : Kurtosis : Minimum : 25th %tile : Median : 75th %tile : Maximum :

Data File: D

Mean : Variance : Std. Dev. : Coef. Var. : Skewness : Kurtosis : Minimum : 25th %tile : Median : 75th %tile : Maximum :

Data File: D

Mean : Variance : Std. Dev. : Coef . Va~f . : Skewness : Kurtosis : Minimum : 25th %tile : Median : 75th %tile : Maximum :

B A T C H S OF CLUSTERED DATA

\F77L\GR0UP1

ASHCOM 2.283 1.259 1.122 49.161

.922 3.997 .390

1.493 2.120 2.900 5.700

\F77L\GROUP2.

ASHCOM 2.601 5.476 2.340

89.965 2.082 6.091 .900

1.350 1.770 2.175 8.780

\F77L\GROUP3

ASHCOM 2.569 1.463 1.210 47.086

.996 3.414 .800

1.700 2.325 3.000 5.720

\F77L\GROUP4

ASHCOM 1.801 1.003 1.001 55.610

.887 2.983 .400 .980

1.500 2.260 4.400

.DAT

SULCOM .248 .007 .084

33.671 1.984 7.221 .160 .190 .230 .273 .570

DAT

SULCOM .352 .016 .127

36.129 .580

2.069 .200 .245 .320 .400 .570

DAT

SULCOM .419 .033 .181

43.100 .932

3.890 .180 .250 .400 .550 .970

DAT

SULCOM .625 .104 .322

51.462 .604

2.760 .150 .330 .600 .800

1.460

T A T I S FROM FIVE

ASHPLY 6.670

10.863 3.296

49.416 .314

2.188 .600

4.150 6.150 9.063

13.510

ASHPLY 13.501 49.635 7.045

52.183 1.055 2.610 7.710 7.890

10.220 15.020 27.050

ASHPLY 7.575

14.394 3.794

50.085 .997

2.872 3.200 5.000 6.635 7.830

16.650

ASHPLY 4.251 2.622 1.619 38.087

.312 1.913 1.360 2.950 3.775 5.670 7.150

T I C S COAL VARIABLES

SULCOM .253 .009 .094

37.120 2.258 7.696 .170 .200 .230 .260 .610

SULCOM .478 .031 .177

37.055 1.002 4.326 .210 .360 .485 .505 .890

SULCOM .435 .039 .197

45.193 .575

2.431 .170 .270 .410 .540 .890

SULCOM .652 .131 .363

55r5"9"5~ .640

2.522 .170 .310 .580 .830

1.530

THICKNESS 6.421 2.271 1.507

23.471 -1.003 3.540 2.400 5.600 6.770 7.387 8.850

THICKNESS 4.960 1.413 1.189

23.964 -.358 2.058 2.990 3.710 5.185 5.545 6.570

THICKNESS 9.637 2.121 1.456

15.113 .598

2.958 7.320 8.390 9.460

10.480 13.400

THICKNESS 5.841 2.066 1.437

"24r60B" -.773 4.982 .460

4.870 6.000 6.670 8.660

stagroup.v5

Table 6.4 Statistical elements for data grouped by five variable Q-mode clustered analysis.

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d

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d

en CO

d CN

CD CO

d

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iri

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CS)

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cn CD CM

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CD 2= (U Q

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55 o o o

APPENDICES

Appendix 3.1 Gamma-ray logs from some drill holes showing variations of fining-upward sequences in the Sangatta Coalfield.

C2290 C2343

Gamma Ray

C2331

Gamma Ray

So

6r

z.r

Jo

ii~

Gamma Ray a» <?r

10a

IOS

"o

Uf

Appendix 3.1 (cont'd)

C2442

C2645

Gamma Ray Gamma Ray

C2S52

Gamma Ray s»

ibS

170

•75-

?s

6a

• 7a

C2695

Appendix 3.1 (cont'd)

Gamma Ray

C2920

Gamma Ray is

S.<0 COAL

Ha

\ ts-

Z.S

C2916

Gamma Ray IS

C3000

Gamm Ray « a* •lO

^o

ly zo

XT

Appendix 3.1 (cont'd)

C3004

Gamma Ray _

C3021

Vo

*r

Gamma Ray 2.ST

3©

Gamma Ray

70

• w

Gamma Ray

• I/O

C3031

Gamma Ray

Appendix 3.1 (cont'd)

'le

<ir

cscu'

Gamma Ray

Gamma Ray

175" XD

. 1S0

C3041

Gamma Ray

70

75"

• <Jo

Appendix 3.1 (cont'd)

C3038

Gamma "ay

iio

C3539

Gamma Ray

.5

•zo

C3538

Gamma Ray

Appendix 3.1 (cont'd)

tiHhi

Gamma Ray Gamma Ray 45

60

65

70

15

50

55

ho

OJ OJ

cn OJ

o

II 11 •3 1 1 II

'; ±m = 1 till

tw

O CO

C

•s ra

•iiOTlMl

LO

cn cn OJ

o

ID OJ

cn OJ

OJ

cn oj CJ

1

i II = 1

1 1

1 II

II

iii 1; 1 in

OJ

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\<z>\ la:1

I CD I

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cn in oj CJ

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=I MMr IH i TT% ; i

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vr

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o o m CJ

to

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m o o ro CJ

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TW 1111111

f,f CTJ^T

tvUlkU

H H m

EXPLANATION

AL ALLUVIliM

DU

BUflNT MUOsrONE

BR BRECCIA

BUflNT SANDSTOR

COAL, lustrous

COAL, nit) lust-oua

COAL, qull lu»troi,B

C4 COAL, nainly tUll with bright bands

CS CQAL, cull witfi ninor brijht bands

C7 COAL, qui] con:hoidal

CF COAL, fusainoua

CONGLOMERArE

CH COAL heat aff,5ct8d/cant>eped

a CLAV

0 •

i-.TT

___

ion a w LitM :'•/"? ••'

• • •

-lief.

MS MUDSTONE

NS NO SAWLE

SA SAND

SC SHALY COAL

SO SANDSTONE

EAT EAflTH

SH SHALE

IILT

SL SILTSTONE

SO SOIL

en SIDERITE

SS SANDSTONE

UO UHOIFFEflENTIATED ROCK TYPE

XN MUDSTONE, carbonaceous

COAL, ^differentiated

CS COflE Lqss

cw COAL, t«eathere^

CY CLAYSTCNE

FW FOSSIL WOOD

CV GRAVEL

IRONSTCNE

KL COflE LQSS

LATERITE

LIMESTQNE

MD MUDSTONE

Vi cd

'—' H O TO

•c w to fi

a a o c iva o ,

11 Xi O

C/3 "^ >-v 0)

O ta

rt o 13 'o

•3 3 60^-i

r 9 ^

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o fi

o

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•IT;

lilt i ° i 1 in 1 1

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> i 1 i ViV i W I V I ' I I Msl 1 1 o

1 tn

1 i

Appendix 3.3 (cont'd)

C2442 C3031

G R LSD G R LSD

Appendix 3.3 (cont'd)

C3041

Gamma Ray Density ^TrOi ,

Appendix 3.4 Palaeocurrent measurements and the correction for tectonic tilt, Sangatta Coalfield.

1 FAXJUEC

1 cinu

(A6,2F7.2, HT-1 HT-1 HT-2 HT-2 HT-2 Bt-3 HT-3 HI-3 HI-3 BT-3 HT-3 HT-3 HT-3 HT-3 HT-3 HT-3 HT-3 HT-3 HT-3 HI-3 HT-1 HT-1 HT-4 HT-1 trr-i HT-1 HT-1 HT-1 HT-1 HT-1 HT-9 HT-9 HT-9 HT-9 RCH-1 RCH-1 RCH-1 RCM-1 RCM-1 RCH-1 ROK-1 RCH-1 RCH-1 ROM-1 RCM-1 RCH-1 RCM-1 HT-6 HT-7 HT-7 HT-7 HT-1 HT-7 HT-7 HT-7 HT-7 EW-7 EW-7 CN-1 CS-2

3. 3. 2.

z. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. 2. Z. 2. 2. 2. 2. 2. 1. 1. 1. 1. 5. 5.

. S.

s. 5. 5. 3. 5. 5. 5. 5. S. 5. Z. 2. 2. 2. 2. 2. 2. 2. 2. 4. 4. 2. 2.

1 1 1 INT MEASUREMENTS. F3.2.A1.

280. 280. 125. 125. 125. 127. 127. 127. 127. 127. 127. 127. 127. 127. 127. 127. 127. 127. 127. 127. 130. 130. 130. 130. 130. 130. 130. 130. 130. 130. 000. ISO. 180. 180. U O . 110. 110. 110. 110. 110. 110. 110. 110. 110. 110. 110. 110. 000. 14S. 145. 145. lis. 145. 145. 145. 145. 345. 345. 220. 157.

00000000000000

oooooooooooooo

P7.2.F6. 20. N 10. N 16.3 1C.9 16.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 13.3 15.3 15.8 15.3 15.3 15.3 15.3 15.3 13.3 15.3 15.3 00. U 11. H 11. u 11. H 15.3 15.3 15.3 15.3 15.3 15.3 15.3 15.3 15.3 15.3 15.3 15.3 15.3 00. E 15.H 15.U 15. U 13. V 15. U 15.W 15.U 15.W 05. E 05.E 10.U 10. V

0 100 5. SANGATTA CCUklFIBLD-JAN/FEB

2,A1) 000. 020. 100. 110. IIS. 030. 040. 045. 035. 060. 020. 02S. 038. 005. 040. 038". 028. 039. 030. 035. 050. 010. 030. 045. 305. 035. 025. OSS. 090. 180. 350. 005. 030. 345. 060. 070. 060. 050. 075. 030. 070. 065. 067. 058. 030. 035. 025. 020. 340. 330. 320. 000. 010. 345. 330. 340. 130. 180. 220. 210.

15. E 15.E 30.3 30. a 30.3 20. E 20. E 20.E 20. E 20.E 20. E 20.E 20. E 25.E 20. E 10. E 30.E 29.E 30.E 20. E 03.3 07. E 03.E 00.3 11. H 00. E 04. E 01. a 11.3 10.H IS. Z 15.E 15. E 15.E 20.3 30.3 20.3 25.3 30.3 20.E 25.3 30.3 30.3 30. S 20. E 20.E 20.Z 15.E 20. E 20. E 20.E 20. E 20. E 20. E 20. E 20.E 30.3 30. U 25.U 20. W

PROGRAMME TO CORRECT CRO33-BE0 MEASUREMENT FOR TECTOHIC TTLT

PAIiAEOCURREHT MEASUREMENTS, SANGATTA COMiFIELD-JAN/FEB 1992

LOCATION STRATIGRAPHIC BEDDING BEDDING X-BED X-BEDDING RESULTANT RESULTANT INTERVAL DIRECTION DIP DIP TREND DIP I-BED TREND Z-BED DIE

HT-1 HT-2

HT-3

HT-9

RCM-1

HT-7

EW-7 CN-1 CM-2

10. 215. 215. 217. 217. 217. 217. 217. 217. 217. 220. 220. 220. 220. 220. 270. 270. 200. ZOO. 200. 200. 200. 200. 200. 235. 235. 235. 235. 75.

310. 277.

20. IS. IS. 13. 13. 13. 13. 13. 13. 13. 15. IS. IS. 15. 15. 0.

11. IS. 15. 15. 15. 15. 15. 15. 15. 15. 15. IS. 5.

10. 10.

90 190 205 130 1ZS 110 128 130 118 120 110 120 35

115 180 80

120 150 150 165 160 157 120, 115. 70. 50.

100 60

220, 310. 300,

15. 30. 30. 20. 20. 20. 20. 20. 30. 30. 3. 3.

14. 4.

11. 15. IS. 20. ZO. 30. 25. 30. ZO. ZO. ZO. 20. 20. 20. 30. 25. 20.

153.50 172. 98 199.69 102.41 98.88 88.64 100.99 102.41 103.21 io4.es 56.66 55.92 42.51 58.74 92.38 83.00 112.75 108.28 108.28 145.88 131.05 135.73 86.11 82.82 68.95 57.02 S6.89 62.98

229.33 315.00 3Z1.30

ZZ.6Z 16.79 11.19 23.13 21.09 26.73 23.52 23.13 31.29 33.89 11.77 15.79 28.97 16.16 9.60

15.00 25.12 15.30 15.30 19.52 16.12 21.38 22.62 23.71 31.70 34.97 32.32 31.97 34.20 15.00 11.15

Appendix 3.4 (cont'd)

NUMBER FREQUENCY DISTRIBUTION

HOC 3TRAT 80 100 120 140 160 ISO 200 220 210 260 280 300 320 340

HT-1 HT-2 HT-3 HT-1 HT-9 RCH-1 HT-7 EW-7 CH-1 CN-2

3. 2. 2. 2. 1. 5. 2. 4. 2. 2.

0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

0.0 0.0 0.0 4.0 0.0 0.0 1.0

o.o 0.0 0.0

0.0 0.0 0.0 0.0 0.0 0.0 2.0 0.0 0.0 0.0

0.0 0.0 0.0 1.0 0.0 0.0 0.0 0.0 0.0 O.O 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 2.0 5.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 2.0 2.0 2.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 1.0 0.0

PERCENTAGE FREQUENCY DISTRIBUTION

IOC STRAT

HT-1

40

0.0 0.0 0.0 HT-2 HT-3 2. 0.0 0.0 0.0 HT-4 2. 0.0 0.0 90.0 HT-9 1. 0.0 0.0 0.0 ROM-1 3. 0.0 0.0 0.0 HI-7 0.0 0.0 25.0

60 80

0.0 0.0 0.0 0.0 0.0 28.6 0.0 20.0 0.0-50.0 0.0 28.6 iO.O 25.0

100

0.0 0.0

71.4 0.0

50.0 28.6 0.0

120

0.0 0.0 0.0 0.0 0.0

28.6 0.0

140

100.0 0.0 0.0 0.0 0.0

14.3 0.0

160

0.0 50.0 0.0 0.0 0.0 0.0 0.0

180 200

0.0 0.0 50.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

220 240 260 280

0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

300

0.0 0.0 0.0 0.0 0.0 0.0 0.0

320 340

0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

EW-7 4. 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 100.0 0.0 0.0 0.0 0.0 0.0 0.0 CN-1 2. 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 100.0 0.0 0.0 CN-2 2. 0.0 0.0 0.0 0,0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0 100.0 0.0

AVERAGES FOR BEDS IH ONE GROUP INTERVAL

LOCATION GROUP BEDS ARITH TREND

VECT TREND

VECT VECT VECT MAGN MAGPC VAR

VECT STD

RAYLE PROS

RAY3IG STAT

AV AV DIP THIOC

3D 3D VECT CONFID APPROX TREND AVDIP KAGNXT CIRCLE PRECIS

HT-1 HT-2 HT-3 HI-4 HT-9 ROM-1 HT-7 EW-7 CN-1 CN-2

1. 2. 7. 5. 2. 7. 4. 1. 1. 1.

153.50 186.33 100.21 61.24 98.87

114.02 68.96 229.33 315.00 324.30

153.50 186.34 100.22 61.00 98.87

114.06 68.91

229.33 315.00 324.30

1.00100 1.9S 97 6.97 99, 4.79 95 1.94 97 6.46 92. 3.92 98 1.00100 1.00100 1.00100.

00 0, 29 356. 62 29. 89 344. 08 385. 34 599. 11 166. 00 0, 00 0. 00 0.

0.00 1.0000 18.89 1.8933 5.43 6.9464 18.35 4.5973 19.62 1.8850 24.48 5.9683 12.91 3.8501 0.00 1.0000 0.00 1.0000 0,00 1.0000

2.2500 2.6229 2.8892 2.84C6 2.6229 2.8892 2.8093 2.2500 2.2500 2.2500

22.62 15.64 26.97 17.12 20.06 19.18 34.24 34.20 15.00 11.45

0.00 0.00

o.oo 0.00

o.oo o.oo 0.00

o.oo o.oo o.oo

153.50 186.41 100.16 61.50 98.42

114.24 69.05 229.33 315.00 324.30

22.62 16.05 27.05 17.80 20.61 20.63 34.73 34.20 15.00 11.45

1.00 1.95 6.96 4.78 1.94 6.52 3.95 1.00 1.00 1.00

0.00 19.80

5.20 135.89 18.37 18.30

0.00 0.00

0.00 17.79 12.30 0.00 0.00 0.00

16.97 12.47 56.73 0.00 0.00 0.00

AVERAGES FOR BEDS IN 100 UNIT INTERVALS

LOCATION 100 INTERVAL AV TREND

HT-1 HT-2 HT-3 HT-1 HT-9 RCM-1 HT-7 EW-7 CN-1 CN-2

0-0-0-0-0-0-0-0-0-0-

99 99 99 99 99 99 99 99 99 99

153.50 186.31 100.22 61.00 98.81

111.06 68.91

229.33 315.00 324.30

;NIT

1.00 1.95 6.97 1.79 1.91 6.16 3.92 1.00 1.00 1.00

MAGNFC

100.00 97.29 99.62 95.89 97.08 92.31 98.11

100.00 100.00 100.00

NO.XBED3

1. 2. 7. 5. 2. 7. 4. 1. 1. 1.

AV DIP

22.62 15.64 26.97 17.12 20.06 19.18 31.21 34.20 IS. 00 11.45

AV THTCX AV GROUP VECT 3 MAGN AGV PC

0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

153.50 186.31 100.22 61.00 98.87

111.06 68.91

229.33 315.00 324.30

100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00 100.00

AVERAGE3 FOR BEDS IN EACH LOCATION

LOCATION AV VECT TREND MAGNIT MAGNFC NO XBEDS AV DIP

HT-1 HT-2 HT-3 HT-1 HT-9 RCH-1 HT-7 EW-7 CN-1 CN-2

153.50 186.31 100.22 61.00 98.87 114.06 68.91 229.33 315.00 321.30

1.00 1.95 6.97 1.79 1.91 6.46 3.92 1.00 1.00 1.00

100 97 99 95 97 92. 98,

100 100 100

.00

.29

.62

.89 ,08 .31 ,11 .00 ,00 .00

kV DIP

22.62 15.61 26.97 17.12 20.06 19.18 34.24 34.20 15.00 11.15

AV THICK

0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

o.oo 0.00

AV GROUP VECT3 MAGN AGV PC

153.50 186.31 100.22 61.00 98.87 111.06 63.91 229.33 315.00 321.30

100.00 100.00 100.00 1D0.00 100.00 100.00 100.00 100.00 100.00 100.00

Appendix 3.5 Thickness data for the Sangatta - Middle interseam deposits.

SANGATTA-MIDDLE SEAMS INTERVAL

DDH EASTING NORTHING THICKNESS m m rn

C2089 98776.40 197896.91 26.96 C2264 99086.46 198701.20 9.79 C2282 97370.20 195055.59 30.88 C2329 98904.90 200228.41 31.82 C2341 97216.58 195589.27 20.72 C2343 98388.37 197435.88 53.04 C2517 98835.53 195505.30 19.81 C2518 98221.68 194515.27 0.33 C2522 97661.33 195438.36 20.78 C2552 96514.24 195987.34 0.45 C2554 96074.91 195750.89 3.49 C2579 96110.64 195500.66 0.82 C2585 98058.92 195009.44 28.92 C2635 98722.02 198249.95 29.20 C2646 98728.14 198581.69 13.41 C2754 101680.79 195229.58 25.01 C2915 98777.81 195251.09 35.77 C2942 101239.44 195215.77 20.87 C3006 96966.24 195487.09 4.26 C3016 98015.11 194496.70 4.75 C3021 97760.92 195013.95 15.02 C3029 97224.10 195376.27 8.8 C3031 97651.76 195194.00 43.8 C3032 97926.21 195242.91 26.58 C3037 97457.62 195272.78 20.52 C3038 97391.71 194879.55 11.54 C3039 97181.80 195127.02 34.62 C3040 97464.08 195498.22 37.86 C3041 97513.03 195746.91 24.56 C3042 97063.44 195746.11 1.52 C3081 98327.73 194756.95 16.90 C3150 98661.34 195258.56 33.79 C3151 98838.15 195377.23 27.50 C3236 98823.58 195301.41 33.60 C3399 98644.70 200254.97 24.91 C3401 97613.91 195127.88 19.86 C3446 98676.00 201463.09 63.18

DDH EASTING NORTHING THICKNESS m m m

C3507 98732.33 195314.32 32.95 C3575 99089.38 198841.57 8.29 C3635 97751.18 194901.69 17.50 C3882 98561.81 195263.45 34.33 C3887 98611.68 195332.97 36.93 F2445 98518.22 195232.06 29.86 F2726 98998.68 198805.84 14.27 F3217 98760.34 195447.98 25.23 F3218 98888.40 195310.94 24.88 F3219 98909.44 195455.73 18.93 F3221 98896.33 195575.09 15.37 F3388 97515.52 195087.89 29.9 C3631 98019.06 194863.54 20.49 C3758 98835.51 195249.16 33.72 F2712 98519.49 195498.53 28.36 F2724 97434.99 194740.31 30.34 C2334 98519.88 195243.70 29.91 C2644 98080.00 194755.25 13.57 C2645 97415.57 196245.17 35.70 C2916 98726.09 195366.94 32.06 C2944 101746.49 194996.20 23.61 C2999 97218.31 195262.02 35.59 C3018 98129.82 194619.98 12.29 C3022 98021.30 194867.52 21.03 C3152 98607.12 195378.94 37.71 C3153 98714.75 195503.20 25.89 C3154 98371.54 195388.59 33.64 C3230 98811.34 195181.59 22.07 C3231 98758.27 195447.16 23.64 C3370 99584.35 203490.88 55.39 C3397 99168.54 200526.55 40.20 C3410 97617.33 195127.55 20.80 C3412 97616.35 195131.64 24.81 C3413 97613.43 195132.42 22.94 C3449 98520.40 200570.17 55.52 C3454 98763.63 199768.66 31.49

Appendix 3.6 Thickness data for the Sangatta - Pinang interseam deposits.

SANGATTA-PINANG SEAMS INTERVAL

DDH EASTING NORTHING THICKNESS DDH EASTING NORTHING THICKNESS

C2282 97370.20 195055.59 68.7 C2290 96712.31 194932.09 45.27 C2332 96716.63 195565.30 50.1 C2341 97216.58 195589.27 58.82 C2343 98388.37 197435.88 98.57 C2442 97689.39 196985.42 58.99 C2518 98221.68 194515.27 60.74 C2521 97612.29 194761.20 54.19 C2522 97661.33 195438.36 56.15 C2635 98722.02 198249.95 64.56 C2643 97767.75 194501.38 61.84 C2644 98080.00 194755.25 61.02 C2942 101239.44 195215.77 46.81 C2985 96805.49 195046.09 46.19 C3001 96277.19 195457.41 46.98 C3003 96399.95 195752.13 50.84 C3004 96675.24 195742.27 19.78 C3005 96806.03 195761.20 36.18 C3015 97829.75 194311.34 49.04 C3016 98015.11 194496.70 69.59 C3017 98389.35 194517.13 54.74 C3019 97580.88 194497.94 48.11 C3020 97740.95 194775.72 53.46 C3021 97760.92 195013.95 55.18 C3022 98021.30 194867.52 65.25 C3031 97651.76 195194.00 76.33 C3037 97457.62 195272.78 58.94

C3040 97464.08 195498.22 74.01 C3041 97513.03 195746.91 66.64 C3042 97063.44 195746.11 54.67 C3391 99187.70 202491.70 79.45 C3392 99215.15 202249.98 65.96 C3393 99294.58 202020.34 59.37 C3395 99265.07 201483.06 67.99 C3399 98644.70 200254.97 50.56 C3400 99505.51 203237.34 57.5 C3401 97613.91 195127.88 52.78 C3410 97617.33 195127.55 53.48 C3443 99916.22 203758.02 77.55 C3445 99260.97 203019.08 86.45 C3446 98676.00 201463.09 82.19 C3493 96836.06 194875.41 43.95 C3536 97599.90 194610.21 51.98 C3538 98226.95 194619.80 63.08 C3539 97655.50 194332.46 51.58 C3634 97914.93 194628.83 63.45 C3635 97751.18 194901.69 59.63 C3637 98228.17 194612.61 63.11 C3641 97652.57 194325.76 51.6 C3704 96258.81 195625.95 43.93 C2444 96510.02 195505.69 42.39 C2717 96479.44 195006.06 48.85 C2724 97434.99 194740.31 42.68

Appendix 3.7 Sand percentage datajbr the Sangatta - Middle and

Sangatta - Pinang interseam_deposits.

DDH

C2646 C2920 C2922 C2926 C3576 C2282 C2518 C2552 C2579 C2916 C2923 C2924 C2982 C2995 C3006 C3007 C3021 C3031 C3038 C3039 C3042 C3154 C3236 C3486 C3631 C3575 C3041 C3634 C3498 C4041 C2713

SANGATTA-MIDDLE INTERVAL EASTING NORTHING

m 98728.14 198581.70 98360.91 195741.60 98194.13 195519.40 99016.59 195505.40 99110.00 198455.00 97370.20 195055.60 98221.68 194515.30 96514.24 195987.30 96110.64 195500.70 98726.09 195366.90 98380.44 195128.30 98725.57 195124.60 96488.47 194598.30 98990.72 195434.40 96966.24 195487.10 96966.18 195359.60 97760.92 195014.00 97651.76 195194.00 97391.71 194879.50 97181.80 195127.00 97063.44 195746.10 98371.54 195388.60 98823.58 195301.40 96239.91 194822.60 98019.06 194863.50 99089.38 197195.60 97513.03 195746.91 97914.93 194628.83 96622.97 195082.38 98908.77 198480.66 98850.83 195856.91

SAND

30.8 8.3 30.8 12.5 10.6 11.1 0.01 0.01 0.01

24.5 35.2 19.2 13.0

SANGATTA-PINANG INTERVAL DDH EASTING NORTHING % SAND

m m

15 0 4

1 01 3

0.01 27.6 0.01 0.01 0.01

36.7 10.5 15.1 5.0 0.01 30.9 6.2 18.1 26.7 0.01

C2646 C2282 C2290 C2331 C2442 C2518 C2984 C3000 C3001 C3002 C3003 C3004 C3020 C3021 C3031 C3038 C3042 C3493 C3496 C3536 C3538 C3539 C3631 C3706 C3575 C3041 C3634 C4041 C2444

98728 97370 96712 96330 97689 98221 96182 96615 96277 96735 96399 96675. 97740. 97760, 97651, 97391, 97063. 96834, 96848, 97599, 98226. 97655, 98019. 96811. 99089. 97513. 97914. 98908. 96510.

.14

.20

.31

.61

.39

.68

.38

.93

.19

.64

.95 ,24 .95 ,92 ,76 ,71 ,44 ,88 ,11 ,90 ,95 50 .06 46 38 03 93 77 02

198581 195055 194932 195022 196985 194515 195126 195246 195457 195382 195752 195742, 194775, 195014, 195194. 194879. 195746. 194874. 195122, 194610. 194619. 194332. 194863. 195490. 197195. 195746. 194628. 198480. 195505.

.70

.60

.10

.40

.40

.30

.00

.00

.40 ,30 .10 .30 ,70 .00 .00 ,50 ,10 ,20 ,10 20 ,80 50 50 80 60 91 83 66 59

25 5

25 39 38 16 23 47 0

24 30 0.

22. 32, 24, 23. 24. 11. 38. 2. 9.

10. 10. 19. 29. 32. 7.

29. 9.

.0

.1

.3

.3

.2

.9

.7

.9

.01

.6

.0

.01

.3

.3

.8 ,6 ,5 ,8 ,7 0 .0 0 0 4 5 2 6 5 2

Appendix 3.8 Thickness and coal quality data for the B2 seam.

DATA FOR B2 SEAM (B2DATA.DAT) DDH

C2331 C2351 C2754 C2942 C2944 C2952 C2983 C3003 C3158 C3486 C3491 C3539 C3641 C3701 R3640 R3695

EASTING m

96330.61 95868.96

101680.79 101239.44 101746.49 102118.77 96463.11 96399.95 98562.94 96239.91 96364.22 97655.50 97652.57 96388.76 97430.30 96415.00

NORTHING m

195022.41 195285.52 195229.58 195215.77 194996.20 195049.44 194871.38 195752.13 195024.02 194822.64 195122.16 194332.46 194325.76 195336.97 194542.98 195320.00

THICKNESS m

1.85 1.80 3.66 2.74 2.86 4.47 2.03 2.40 2.70 1.50 1.80 2.09 1.85 1.59 0.76 1.47

ASH °o

10.49 8.81

13.37 6.04

11.85 11.87 7.43

10.08

8.62 10.04

SUI ,PH' °0

0, 0, 0, 0. 1, 0 0.

0

0 0

,26 .54 .46 ,49 ,53 .21 .20

.24

.24

.26

Appendix 6.1 Computer program (Fortran-77L) LIMIT.

PROGRAM LIMIT C PROGRAM TO LIMIT DATA ACCORDING TO A BLOCK

DOUBLE PRECISION XDATA(2000),YDATA(2000),WDATA(2000),ZDATA(2000) COMMON/SYS/FILE NAMELIST/lmt/FNAME,BLKDIM,FORMT CHARACTER FNAME*17,FORMT*80,C*1,FN*17 OPEN(18,FILE='hmit.nml',STATUS='OLD*) READ(18,lmt) PRINT/LIMIT THE DATA BY THEIR CO-ORDINATES (Y/N)?: ' READ(*,99)C

99 FORMATCA1) IF(C.EQ.'N'.OR.C.EQ.'n') GOTO 9999

C ******* LIMIT DATA POINTS ****** WPJTE(6,43) READ(5,*)XXW WRITE(6,44) READ(5,*)XXE WRITE(6,45) READ(5,*)YYS WRITE(6,46) READ(5,*)YYN

Q ************ READ LIMITED DATA ************************ OPEN(20,FILE=FNAME,STATUS=*OLD',ACCESS='SEQUENTIAL') REWIND 20 NDATA=1

200 READ(20,FORMT,END=300)XDATA(NDATA),YDATA(NDATA),WDATA(NDATA) 1 ZDATA(NDATA) ' IF(XDATA(NDATA).EQ.0.0.OR.ZDATA(NDATA).EQ.0.0) goto 200 IF(XDATA(NDATA).LT.XXW.OR.XDATA(NDATA).GT.XXE)GO TO 200 IF(YDATA(NDATA).LT.YYS.OR.YDATA(NDATA).GT.YYN)GO TO 200 ndata=ndata+l

250 GOTO 200 300 CLOSE(UNIT=20)

NDATA=NDATA-1 310 WRTTE(*,350)NDATA 350 FORMAT(lX,'NUMBER OF DATA POINTS= ',15)

PRINT, 'OUTPUT FILE', FN READ(*,*)FN OPEN(UNIT=2,FILE=FN) DO 360 I=1,NDATA

WRITE(2,100)XDATA(I),YDATA(I),WDATA(I),ZDATA(I) 360 CONTINUE

CLOSE(UNIT=2) 43 FORMATC1X,' WEST LIMIT OF DATA = ') 44 FORMATC1X,' EAST LIMIT OF DATA = ') 45 FORMATC1X,' SOUTH LIMIT OF DATA= ') 46 FORMATC1X,' NORTH LIMIT OF DATA= ') 100 FORMATC4F10.2) 9999 stop END

Appendix 6.2 Computer program (Fortran-77L) WIND.

PROGRAM WIND C********************************************************************** c C THIS PROGRAM IS TO SET 2-D WINDOW FOR DRILLHOLE DATA C C PROGRAM WAS WRITTEN BY C C. NAS C DEPARTMENT OF GEOLOGY C UNIVERSITY OF WOLLONGONG C AUSTRALIA C C LAST MODIFIED ON FEBRUARY, 1991 C THIS PROGRAM USES TWO OPTIONAL SEARCHING METHODS OF EACH WINDOW: C 1. CIRCLE; AND C 2. RETANGLE C ********************** KEY VARIABLES ******************************** C VARIABLE DESCRIPTION c

C X EASTING COORDINATE C Y NORTHING COORDINATE C GRADE COAL SEAM PARAMETER (ASH, SULFUR,THICKNESS, ETC) C WIDX WIDTH OF WINDOWS ALONG X AXES (IF RETANGLE) C WIDY WIDTH OF WINDOWS ALONG Y AXES (IF RETANGLE) C RMAX RADIUS OF WINDOWS (IF CIRCLE) C XIN INCREMENT OF X C YIN INCREMENT OF Y C XC EASTING COORDINATE OF CENTRE OF WINDOWS C YC NORTHING COORDINATE OF CENTRE OF WINDOWS C NX NUMBER OF GRIDS ALONG X-AXIS C NY NUMBER OF GRIDS ALONG Y-AXIS C FORMT FORMAT OF DATA FILE READ BY WINDOW C NHOL NUMBER OF DRILLHOLES C WIND.NML NAMELIST FILE CONTAINING DATAFILE NAME C ********************************************************************* C

COMMON/NAS1/HOLID(2500) ,Y(2500) ,X(2500) ,GRADE(2500) COMMON/OFF/XOF,YOF ,XST1 ,YST1 ,XXW ,XXE ,YYS ,YYN ,XW ,XE ,YS ,YN ,NX ,NY NAMELIST/wnd/FNAME,FORMT.BLKDIM DATA MAXD,XMIN,YMIN,GRADEMIN/2500,9999999.,9999999., 999999./ DATA XMAX,YMAX.GRADEMAX/-9999999.,-999999.,-999999./ CHARACTER C*l,HOLID*10,FNAME*15,FORMT*50,FN*15

C ***************************************************************** PRINT,* THE PROGRAM REQUIRES TWO DATA FILES:' PRINT,' ' PRINT,' <1> RUN PARAMETERS IN wind.nral FILE' PRINT,' <2> ASSAY DATA FILE ' PRINT,' ' PRINT,' enter X to exit OR ' PRINT, ' ANY KEY to continue > ' READ(*,5)C

5 FORMAT(Al) IF(C.EQ.'X'.OR.C.EQ.'x') STOP

C ******************************************************* OPEN(18,FILE='wind.nml',STATUS='OLD') READ(18,wnd) PRINT,'WRITE OUTPUT FILE NAME ?' ,FN READ(*,*)FN OPEN(19 ,FILE=FN ,STATUS= 'UNKNOWN' ,ACCESS= ' SEQUENTIAL * ) OPEN(20,FILE=FNAME,STATUS= 'OLD' ,ACCESS= 'SEQUENTIAL')

C C READ DATA - CALL ROUTINE RDATA C

CALL RDATA(FORMT,MAXD,NHOL,XMIN ,XMAX,YMIN,YMAX.GRADEMIN.GRADEMAX) C

WRITE(6,10) WRITE(6,12) READ(*,15)B

10 FORMAT(IX,'SEARCHING METHOD?: ') 12 FORMAT(IX,'CIRCLE= 1 ; RETANGLE= 2 ') 15 FORMAT(Il)

IF(B.EQ.l) GOTO 20 CALL RETANG(NHOL,WIDX,WIDY,XIN,YIN) GOTO 30

20 CALL RADIAL(NHOL,XIN,YIN,RMAX) 30 STOP

END C C ******** SUBROUTINE RETANG TO SET RETANGLE WINDOWS *************

SUBROUTINE RETANG(NHOL,WIDX,WIDY,XIN,YIN) C ****************************************************************

Appendix 6.2 (cont'd)

COMMON/NAS1/HOLID(2500),Y(2500),X(2500),GRADE(2500) COMMON/OFF/XOF ,YOF ,XST1 ,YST1 ,XXW ,XXE ,YYS ,YYN ,XW ,XE ,YS ,YN ,NX,

CHARACTER HOLID*10 C

WRITE(6,5) READ(*,*)XW WRITE(6,6) READ(*,*)XE WRITE(6,7) READ(*,*)YS WRITE(6,8) READ(*,*)YN

5 FORMAT(IX,'WEST LIMIT OF GRID = ') 6 FORMAT(IX,'EAST LIMIT OF GRID = *) 7 FORMAT(IX,'SOUTH LIMIT OF GRID= ') 8 FORMAT(IX,'NORTH LIMIT OF GRID= ') C **** INCREMENTS ****

WRITE(6,9) READ(*,*)WIDX WRITE(6,10) READ(*,*)WIDY

9 FORMATdX, 'WIDTH OF WINDOWS ALONG X-AXIS= ') 10 FORMATdX,'WIDTH OF WINDOWS ALONG Y-AXIS= ') C

WRITE(6,11) READ(*,*)XIN WRITE(6,12) READ(*,*)YIN PRINT,' '

11 FORMAT(IX,'MOVING INCREMENTS ALONG X-AXIS= ') 12 FORMATdX,'MOVING INCREMENTS ALONG Y-AXIS= *)

nx =(XE-XW)/XIN ny =(YN-YS)/YIN PRINT, 'NUMBER OF GRID ALONG X-AXIS =',NX PRINT, 'NUMBER OF GRID ALONG Y-AXIS =',NY

C do 20 K = l,(ny) do 20 L = 1, (nx) xl=XW+xin*(L-l) x2=xl-(widx/2) X3=Xl+(WIDX/2) yl=YS+yin*(K-l) y2=yl-(widy/2) Y3=Yl+(WIDY/2)

C C ***** SEARCHING DATA WITHIN EACH BLOCK ***** C

NDAT=0 SUM1=0.0 SUM2=0.0 XMEAN=0. COEF=0. VAR=0.

C C LOOP AND COLLECT WINDOW STATISTICS C

DO 25 1 = 1,NHOL IF(X(i).LT.X2.0R.X(i).GT.X3) GOTO 25 IF(Y(i).LT.Y2.0R.Y(i)«GT.Y3) GOTO 25 SUMl = SUM1+GRADE(I) SUM2= SUM2+GRADE(I)*GRADE(I) NDAT=NDAT+1

25 CONTINUE C

if(NDAT.lt.5) go to 20 C

XMEAN= SUMl/FLOAT(NDAT) SUB=SUM2-(SUMl*SUM1)/FLOAT(NDAT) VAR= SUB/FLOAT(NDAT-1) STD=SQRT(VAR) COEF=STD/XMEAN xc=xl yc=yl

c WRITE (19,30)xc,yc,NDAT,XMEAN,COEF,STD

20 CONTINUE 30 FORMAT (6F10.2)

RETURN END

C ************************************************

Appendix 6.2 (cont'd)

SUBROUTINE RADIAL(NHOL ,XIN ,YIN,RMAX) C ************************************************

COMMON/NAS1/HOLID(2500) ,Y(2500),X(2500),GRADE(2500) COMM0N/OFF/X0F ,YOF ,XST1 ,YST1 ,XXW ,XXE ,YYS ,YYN ,XW ,XE ,YS ,YN ,NX ,NY CHARACTER HOLID*10

C WRITE(6,5) READ(*,*)XW WRITE(6,6) READ(*,*)XE WRITE(6,7) READ(*,*)YS WRITE(6,8) READ(*,*)YN

5 F0RMAT(1X,'WEST LIMIT OF GRID = ') 6 FORMAT(IX,'EAST LIMIT OF GRID = *) 7 F0RMAT(1X,'SOUTH LIMIT OF GRID= ') 8 FORMAT(IX,'NORTH LIMIT OF GRID= ')

WRITE(6,11) READ(*,*)XIN WRITE(6,12) READ(*,*)YIN PRINT,' '

11 FORMAT(IX,'MOVING INCREMENTS ALONG X-AXIS= ') 12 FORMATdX,'MOVING INCREMENTS ALONG Y-AXIS= ')

nx =(XE-XW)/XIN ny =(YN-YS)/YIN PRINT,'NUMBER OF GRIDS ALONG X-AXIS=',NX PRINT,'NUMBER OF GRIDS ALONG Y-AXIS=' ,NY

WRITE(6,13) READ(*,*)RMAX

13 FORMATdX, 'RADIUS OF SEARCHING: ') C

do 20 K = l,(ny) do 20 L = 1,(nx) xl=XW+xin*(L-l) yl=YS+yin*(K-l)

C C ***** SEARCHING DATA WITHIN EACH BLOCK ***** C

NDAT=0 SUMl=0.0 SUM2=0.0 XMEAN=0. C0EF=0. VAR=0.

C C LOOP AND COLLECT WINDOW STATISTICS C

DO 25 1 = 1,NHOL D=(((X(I)-X1)**2)+((Y(I)-Y1)**2))**0.5 IF(D.GT.RMAX) GOTO 25 SUMl = SUMl+GRADE(I) SUM2= SUM2+GRADE(I)*GRADE(I) NDAT=NDAT+1

25 CONTINUE C

if(NDAT.It.5) go to 20 C

XMEAN=SUMl/FLOAT(NDAT) SUB=SUM2-(SUMl*SUM1)/FLOAT(NDAT) VAR=SUB/FLOAT(NDAT-1) STD=SQRT(VAR) COEF=STD/XMEAN xc=xl yc=yl

WRITE (19,30)xc,yc,NDAT,XMEAN,COEF,STD 20 CONTINUE 30 FORMAT (6F10.2)

RETURN END

r ********************* SUBROUTINE RDATA ***************************** SUBROUTINE RDATA(FORMT,MAXD,NHOL,XMIN,XMAX.YMIN.YMAX

1.GRADEMIN.GRADEMAX) c****;;**;**********************************************""***" c

THIS ROUTINE READS DATA AND DETERMINE MAXIMUM/MINIMUM COORD

C****************** ********************************************** COMMON/NASl/HOLID(2500),Y(2500),X(2500),GRADE(2500)

Appendix 6.2 (cont'd)

COMMON/OFF/XOF ,YOF ,XSTl ,YST1 ,XXW ,XXE ,YYS , YYN ,XW ,XE ,YS , YN ,NX ,NY

CHARACTER HOLID*10,FORMT*50,C*1 PRINT,'LIMIT THE DATA BY THBIR CO-ORDINATES (Y/N)?: ' READ(*,10)c

10 FORMAT(Al) IF(C.EQ.'N'.OR.C.EQ.'n') GOTO 22

C ******* LIMIT DATA POINTS ****** WRITE(6,43) READ(5,*)XXW WRITE(6,44) RBAD(5,*)XXE WRITE(6,45) HEAD(5,*)YYS WRITE(6,46) READ(5,*)YYN 1 = 1

20 READ(20,FORMT,END=21) X(I),Y(I),GRADE(I) C C ZERO GRADE & COORDINATES ARE ASSUMED TO BE BLANK LINE C

IF(X(I).EQ.0.0.OR.GRADE(I).EQ.0.0) GO TO 20 IF(X(I).LT.XXW.OR.X(I).GT.XXE)GO TO 20 IF(Y(I).LT.YYS.0R.Y(I).GT.YYN)GO TO 20 IF(Xd).LT.XMIN) XMIN=X(I) IF(X(I).GT.XMAX) XMAX=X(I) IF(Y(I).LT.YMIN) YMIN=Y(I) IF(Y(I).GT.YMAX) YMAX=Y(I) IF(GRADE(I).LT.GRADEMIN) GRADEMIN=GRADE(I) IF(GRADE(I) .GT.GRADEMAX) GRADEMAX=GRADE(I) 1 = 1+1 IF(I.LE.MAXD) GO TO 20 PRINT,*** DATA ALLOWED EXCEEDED - ONLY FIRST ',MAXD,' USED'

21 CONTINUE GO TO 40

C****** READ ALL DATA ********** 22 1 = 1 23 READ(20,FORMT,END=24) X(I),Y(I),GRADE(I)

IF(X(I).EO.0.0.OR.GRADE(I).EQ.0.0) GO TO 23 IF(X(I).LT.XMIN) XMIN=X(I) IF(X(I).GT.XMAX) XMAX=X(I) IF(Y(I).LT.YMIN) YMIN=Y(I) IF(Y(I).GT,YMAX) YMAX=Y(I) IF(GRADE(I).LT.GRADEMIN) GRADEMIN=GRADE(I) IF(GRADE(I).GT.GRADEMAX) GRADEMAX=GRADE(I) 1 = 1+1 IF(I.LE.MAXD) GO TO 23 PRINT,*** DATA ALLOWED EXCEEDED - ONLY FIRST '.MAXD,' USED1

24 CONTINUE C 40 NHOL=I-l C C DEBUG STATEMENTS C

PRINT,'NUMBER OF DATA POINTS=',NHOL PRINT,*XMIN=',XMIN,'XMAX=',XMAX PRINT,'YMIN=',YMIN,'YMAX=',YMAX PRINT,'VALUE MIN=•.GRADEMIN,'VALUE MAX='.GRADEMAX PRINT, ' '

43 FORMATdX,' WEST LIMIT OF DATA = ') 44 FORMATdX,' EAST LIMIT OF DATA = ') 45 FORMATdX,' SOUTH LIMIT OF DATA= ') 46 FORMATdX,' NORTH LIMIT OF DATA= ')

C RETURN END

Appendix 6.3 Computer program (Fortran-77L) TREND.

PROGRAM TREND C ****************************************************************** C THIS PROGRAM IS DEVELOPED BY C. N A S BASED ON THE HIGH SPEED C MATRIX GENERATOR (HSMG) ALGORITM FOR SURFACE FUNCTION WRITTEN BY C P. J BALCH AND T.H THOMPSON (1989). C LAST MODIFICATION IN SEPTEMBER 1992, PARTICULARLY IN: C 1. INPUT DATA SYSTEM: - RUN DIFFERENT VARIABLES FROM ONE FILE C - TWO OPTIONS, USE ALL DATA OR LIMIT THE C DATA BY COORDINATES, CONTROLED BY C "SUBROUTINE RDATA" C - USER DTERMINED GRIDING BORDER C 2. NAHELIST CONTROL FILE: "TREND.NML" FILE CONTROL INPUT DATA AND C THE FORMAT C 3. ADDITIONAL GRIDED COORDINATES FILE SUBROUTINE: ENABLE TO CALCULATE C Z-VALUES IN GRIDED POINTS. TEMPORARY GRID.DAT C FILE IS GENERATED C 4. COMPUTATION OF CALCULATED Z-VALUES IN GRIDED DATA: THE RESULTS ARE C STORED IN FILES READY TO BE CONTOURED BY "SURFER" C 5. ADDITIONAL SIMPLE COMPUTATION SUCH AS F TEST AND RESIDUAL VALUES IN C DATA POINTS: OUTPUT FILES FOR RESIDUAL MAPS C ******************************************************************

DOUBLE PRECISION MATRIX(66,67) ,HSMG(21,21),SURF(11,11) DOUBLE PRECISION ZADD(11,11),X,Y,Z,XA(66),Z1,A,F DOUBLE PRECISION XDATA(2000),YDATA(2000),ZDATA(2000) DOUBLE PRECISION U(8000),V(8000),AA(8000) DOUBLE PRECISION XW.XE.YS.YN.XD.YD INTEGER *2 I,J,K,L,M,N,NDEG,NDEG1.NDEG2,NALF.NALF1.NALF2 INTEGER *2 II,NROW,NCOL,NDATA,NGRID,G,H COMMON/SYS/FILE NAMELIST/srf/FNAME.BLKDIM,FORMT CHARACTER FNAME*17,FNAMEA*17,FNAMEB*17,FNAMEC*17,W*1,FORMT*80 CHARACTER C*l COMMON XA.NDEG.NDEG1.NDEG2,HSMG,ZADD,SURF OPEN(18,FILE='TREND.NML'.STATUS='OLD') READ(18,srf)

C PRINT,' *********************************************************' PRINT,'TREND SURFACE ANALYSIS PROGRAM' PRINT,'LAST MODIFICATION BY C. NAS SEPTEMBER 1992' PRINT,' ' PRINT,' THIS PROGRAM REQUIRES : ' PRINT,' 1. NAMELIST CONTROL FILE, "SURFACE.NML" ' PRINT,' 2. DATA FILE, FORMAT CONTROLED FROM "SURFACE.NML" ' PRINT.' ' PRINT,' FOUR FILES ARE CREATED AT ONCE: COEF. FILE, GRIDED-Z ' PRINT,' VALUES FILE, RESIDUAL FILE AND GRID.DAT FILE.' PRINT,' GRIDED-Z FILE IS READY TO BE CONTOURED BY "SURFER"' PRINT,' ' PRINT,' PLEASE FOLLOW THE INSTRUCTION CAREFULLY, GOOD LUCK !! ' PRINT,' IF NOT READY PLEASE PRESS Ctl-C AND PREPARE THE FILES ' PRINT,'*********************************************************' PRINT,' '

200 print,'NEW DATA (Y) OR OTHER DEGREES (N) ?: ' READ(*,250)C

250 FORMAT(Al) IF(C.EQ.'N'.OR.C.EQ.'n') GOTO 360

300 CALL RDATA(XDATA,YDATA,ZDATA,NDATA,FNAME,FORMT,ZMIN,ZMAX 1,xmax,xmin,ymax,ymin)

C ************************ CREATE GRID FILE *********************** 305 CALL GRID(xmax,xmin,ymax,ymin,XW,XE,YS,YN,G,H,XD,YD) C ***************************************************************** 306 OPEN(UNIT=2,FILE='GRID.DAT')

REWIND 2 NGRID=1

350 READ(2,*,END=351)U(NGRID),V(NGRID) NGRID=NGRID+1 GOTO 350

351 CLOSE(UNIT=2) NGRID=NGRID-1 WHITE(6,52)NGRID

C ******************* COMPUTE DO-LOOP INDICES ******************* 360 WRITE(6,40)

READ(5,35)FNAMEA WRITE(6,41) READ(5,35)FNAMEB WRITE(6,42) READ(5,35)FNAMEC

C PRINT,' ORDER OF TREND SURFACE ? : ' READ(5,*,ERR=360)NDEG

Appendix 6.3 (cont'd)

IF ((NDEG.GT.IO).OR.(NDEG.LE.O)) WRITE(6,25) IF ((NDEG.GT.IO).OR.(NDEG.LE.O)) GOTO 360

NDEG1=NDEG+1 NDEG2=NDEG+2 NROW=NDEG1*NDEG2/2 NCOL=NROW+1

400 NALF=2*NDEG NALF1=NALF+1 NALF2=NALF1+1

C ********************** INITIALIXE ARRAYS ********************** DO 500 I=1,NALF1 DO 500 J=1,NALF2-I

500 HSMG(I,J)=O.0D+00 DO 600 1=1,NDEG1 DO 600 J=1,NDEG2-I

600 ZADD(I,J)=O.OD+00 WRITE(6,*)' SETTING UP HIGH SPEED MATRIX GENBRATOR '

C ***************** EVALUATE ZERO DEGREE SURFACE **************** Zl=0.0D+0O DO 700 I=1,NDATA

700 Z1.= Z1+ZDATA(I) IF (NDEG.EQ.O) GOTO 1200

C **************** COMPUTE VALUES FOR HSMG MATRIX *************** DO 1100 I=1,NDATA

A=1.0D+00 XA(l)=1.0D+00 X=XDATA(I) Y=YDATA(I) Z=ZDATA(I)

DO 800 J=2,NALF1 A=A*X XA(J)=A IF(J.LE.NDEGl) ZADD(1,J)=ZADD(1,J)+A*Z

800 HSMG(1,J)=HSMG(1,J)+A DO 1100 L=2,NALF1 DO 900 M=1,NALF2-L

XA(M)=XA(M)*Y 900 HSMG(L,M)=HSMG(L,M)+XA(M)

IF (L.GT.NDEG1) GOTO 1100 DO 1000 N=l.NDEG2-L

1000 ZADD(L,N)=ZADD(L,N)+XA(N)*Z 1100 CONTINUE 1200 HSMG(1,1)=DBLE(NDATA)

ZADD(1,1)=Z1 C ******************** CALL SUBROUTINE SOLVE ******************** 1300 CALL SOLVE(MATRIX,NROW,NCOL)

C ****** REORDER COEFFICIENTS FOR OUTPUT FILE AND FUNCTION ****** K=0

DO 1400 1 = 1 .NDEG1 DO 1400 J=1,NDEG2-I

K=K+1 1400 SURF(I,J)=XA(K)

C ******************* INSERT OUTPUT ROUTINE HERE **************** C ****** OUTPUT SURFACE EXPANSION COEFFICIENTS

WRITE(6,*)' GENERATING OUTPUT FILES ' OPEN(UNIT=l,FILE=FNAMEA) REWIND 1

WRITE(1,*)' Z=F(X,Y) SURFACE EXPANSION COEFFICIENTS ' WRITE(1,*)' INCREASING DEGREE AND DECREASING POWERS OF X '

DO 1500 I=1,NDEG1 11=1+1 WRITE(1,75) 1-1

1500 WRITE(1,80) ((SURF(J,I1-J)) ,J=1,1) CLOSE(UNIT=1)

C ******** OUTPUT X,Y,SURFACE Z-VALUES C *************************************************************

OPEN(UNIT=l,FILE=FNAMEB) REWIND 1

WRITE(1,1602) WRITE(1,*)(G+1),(H+1)

WRITE(1,1603)XW,XE WRITE(1,1603)YS,YN WRITE(1,1603)ZMIN,ZMAX DO 1600 L=1,NGRID

AA(L)=F(U(L),V(L)) C WRITE(*,*)U(L),V(L),AA 1600 CONTINUE

WRITE(1,1604)(AA(L), L=l,NGRID) CLOSE(UNIT=1)

1602 FORMAT('DSAA')

Appendix 6.3 (cont'd)

1603 FORMAT(2F10.2) 1604 F0RMAT(15(F8.2,1X)) C ********************************************

DO 1700 1=1.NDATA B=F(XDATA(I),YDATA(I)) Re=(ZDATA(I)-B) ndd=(1.5*NDEG)+(0.5*(ndeg**2))

OPEN(UNIT=l,FILE=FNAMEC) WRITE(l,1710)XDATA(I),YDATA(I),ZDATA(I),B,Re

1700 CONTINUE 1710 FORMAT(2X.5F10.2)

call £it(Fnamec,ndd,Xdata,Ydata,Zdata,b) WRITE(6,95) READ(5,97) W IF (W.EQ.'N'.OR.W.EQ.'n') GOTO 9999

C ************************ FORMAT STATEMENTS ******************** 25 FORMATdX,' ERROR! OUT OF RANGE. MIN. = 1, MAX. = 10',/) 35 FORMAT(Al7) 40 F0RMAT(1X,' NAME OF OUTPUT FILE FOR EQUATION COEFFICIENT: ') 41 F0RMAT(1X,' NAME OF OUTPUT FILE FOR GRIDED-Z VALUES: ') 42 F0RMAT<1X,' NAME OF OUTPUT FILE FOR RESIDUAL VALUES: ') 50 F0RMAT(1X,/,IX,' NUMBER OF DATA POINTS =',I7,/) 52 FORMATdX,/,IX,' NUMBER OF GRID POINTS =',I7,/) 75 F0RMAT(1X,/,IX,'TERMS = ',13) 80 FORMATdX, 50(T2,1PD23.15,T36.1PD23.15,T70.1PD23.15,T104.1PD23

+.15:/)) 95 FORMATdX,/,IX,' ANOTHER RUN (Y/N)?: ') 97 FORMAT(A)

GO TO 200 9999 END

C ************************ SUBROUTINE SOLVE ********************* SUBROUTINE SOLVE(MAT,NROW,NCOL) INTEGER*2 I,J,K,L,M,N,NDEG,NDEG1 ,NDEG2,NB,Il,NROW,NCOL,KI INTEGER*2 NR1,NL DOUBLE PRECISION HSMG(21,21),ZADD(11,11),SURF(11,11) DOUBLE PRECISION MAT(NROW.NCOL).CONST.SAVE,AMAX,XA(66) ,SUM COMMON XA,NDEG.NDEGl,NDEG2,HSMG,ZADD,SURF

C C ***** SET UP COEFFICIENT MATRIX

M=0 DO 100 I=1,NDEG1 DO 100 J=1,NDEG2-I

N=0 M=M+1

MAT(M,NCOL)=ZADD(I,J) DO 100 K=I.NDEG+I DO 100 L=J .NDEG+I+J-K

N=N+1 100 MAT(M,N)=HSMG(K,L)

WRITE(6,200) 200 FORMATdX,/,IX,* SOLVING COEFFICIENT MATRIX.')

C ***** SOLVE COEFFICIENT MATRIX IF (NDEG.EQ.O) XA(1)=MAT(1,2)/MAT(l.1) IF (NDEG.EQ.O) RETURN NR1=NR0W-1

DO 700 K=1,NR1 C ***** FIND LARGEST VALUE IN COLUMN FOR PIVOT, INTERCHANGE ROW

NB=0 AMAX=MAT(K,K) I1=K+1

DO 300 KI=I1,NR0W IF (DABS(MAT(KI,K)).LE.DABS(AMAX)) GOTO 300 AMAX=MAT(KI,K) NB=KI

300 CONTINUE IF (NB.EQ.O) GOTO 500

DO 400 NL=K,NCOL SAVE=MAT(NB,NL) MAT(NB,NL)=MAT(K,NL)

400 MAT(K,NL)=SAVE C ***** USE COLUMN ORIENTED GAUSS ELIMINATION

500 CONST=MAT(K,K) DO 600 I=I1,NR0W

600 XA(I)=-MAT(I,K)/CONST DO 700 J=Il,NCOL

CONST=MAT(K,J) DO 700 I=I1,NR0W

700 MAT(I,J)=MAT(I,J)+CONST*XA(I) C ***** BACK SUBSTITUTE

XA(NROW)=MAT(NROW,NCOL)/MAT(NROW,NROW)

Appendix 6.3 (cont'd)

DO 900 I=1,NR1 K=NROW-I SUM=O.0D+0O CONST=MAT(K,K)

DO 800 J=1+K,I+K 800 SUM=SUM+MAT(K,J)*XA(J) 900 XA(K.)=(MAT(K,NCOL)-SUM) /CONST

RETURN END

C***************** SUBROUTINE GRID *********** SUBROUTINE GRID(xax,xin,yax,yin,XW,XE,YS,YN,G,H,XD,YD) DOUBLE PRECISION XDATA(2000),YDATA(2000) DOUBLE PRECISION XW.XE.YS,YN,XD,YD INTEGER *2 G,H,J,K,M,N character c*l print,'limit the grids (y/n)?: ' READ(*,50)C

50 FORMAT(Al) IF(C.EQ.'N*.OR.C.EQ.'n') GOTO 251

c****** DETERMINE WIDTH OF MAP **** WRITE(6,*) WRITE(6,100) READ(*,*)XW WRITE(6,150) READ(*,*)XE WRITE(6,200) READ(*,*)YS WRITE(6,250) READ(*,*)YN

100 FORMAT(IX,'WEST LIMIT OF GRID = ') 150 FORMAT(IX,'EAST LIMIT OF GRID = ') 200 FORMAT(IX,'SOUTH LIMIT OF GRID= ') 250 F0RMAT(1X,'NORTH LIMIT OF GRID= *)

WIDX=XE-XW WIDY=YN-YS go to 252

C **** INCREMENTS **** 251 write(*,*)xax,xin,yax,yin

widx=xax-xin widy=yax-yin

c write(*,*)widx,widy 252 WRITE(6,260)

READ(*,*)XD WRITE(6,270) READ(*,*)YD

260 FORMATdX, 'WIDTH OF GRIDS ALONG X-AXIS= ') 270 FORMAT(IX,'WIDTH OF GRIDS ALONG Y-AXIS= *)

G=WIDX/XD H=WIDY/YD

C ****** DETERMINE COORDINATE OF GRID ***** DO 300 J=0,H DO 350 K=0,G XDATA(K)=XW+(XD*K) YDATA(J)=YS+(YD*J)

350 CONTINUE 300 CONTINUE C ***** STORE RESULT IN GRIDED DATA FILE *******

OPEN(UNIT=2,FILE='GRID.DAT') REWIND 2 DO 400 M=0,H DO 400 N=0,G

C WRITE(*,1000)XDATA(N),YDATA(M) WRITE(2,1000)XDATA(N),YDATA(M)

400 CONTINUE CL0SE(UNIT=2)

1000 FORMAT(2X,2F12.2) RETURN END

C ********************SURFACE FUNCTION *************** DOUBLE PRECISION FUNCTION F(X,Y) DOUBLE PRECISION HSMG(21,21),ZADD(11,11),SURF(11,11) DOUBLE PRECISION X,Y,XA(66),Y1,A INTEGER *2 I.J.NDEG.NDEGl,NDEG2 COMMON XA,NDEG,NDEG1,NDEG2,HSMG,ZADD,SURF

C IF (NDEC.EQ.O) F=SURF(1,1) IF (NDEG.EQ.O) RETURN A=1.0D+00 Yl=0.0D+00 XA(l)=1.0D+00

Appendix 6.3 (cont'd)

DO 100 I=2,NDEG1 A=A*X

XA(I)=A 100 Y1=Y1+A*SURF(1,I)

DO 200 I=2,NDEG1 DO 200 J=l.NDEG2-I

XA(J)=XA(J)*Y 200 Y1=Y1+XA(J)*SURF(I,J)

F=Y1+SURF(1,1) RETURN END

C***************** READ DATA *************************************** SUBROUTINE RDATA(XDATA,YDATA,ZDATA,NDATA,FNAME,FORMT 1 ,ZMIN ,ZMAX ,xmax .xmin.ymax .ymiri) DOUBLE PRECISION XDATA(2000),YDATA(2000),ZDATA(2000)

1,ZDATAMIN,ZDATAMAX DOUBLE PRECISION XXW.XXE.YYS,YYN CHARACTER FNAME*17,FORMT*80,C*1 DATA XDATAMIN.YDATAMIN/9999999.,9999999./ DATA XDATAMAX.YDATAMAX/-9999999.,-9999999./ DATA ZDATAMIN,ZDATAMAX/9999999.,-9999999./ PRINT,'LIMIT THE DATA BY THEIR CO-ORDINATES (Y/N)?: ' READ(*,99)C

99 FORMAT(Al) IF(C.EQ.'N'.OR.C.EQ.'n') GOTO 301

C ******* LIMIT DATA POINTS ****** WRITE(6,43) READ(5,*)XXW WRITE(6,44) READ(5,*)XXE WRITE(6,45) READ(5,*)YYS WRITE(6,46) READ(5,*)YYN

C ************ READ LIMITED DATA ************************ OPEN(20,FILE=FNAME,STATUS= 'OLD',ACCESS='SEQUENTIAL')

REWIND 20 NDATA=1

200 READ(20,FORMT,END=300) XDATA(NDATA).YDATA(NDATA),ZDATA(NDATA) IF(XDATA(NDATA).EQ.0.0.OR.ZDATA(NDATA).EQ.0.0) goto 200 IF(XDATA(NDATA).LT.XXW.OR.XDATA(NDATA).GT.XXE)GO TO 200 IF(YDATA(NDATA).LT.YYS.OR.YDATA(NDATA).GT.YYN)GO TO 200

IF(XDATA(NDATA).LT.XDATAMIN) XDATAMIN=XDATA(NDATA) IF(XDATA(NDATA).GT.XDATAMAX) XDATAMAX=XDATA(NDATA) IF(YDATA(NDATA).LT.YDATAMIN) YDATAMIN=YDATA(NDATA) IF(YDATA(NDATA).GT.YDATAMAX) YDATAMAX=YDATA(NDATA) IF(ZDATA(NDATA).LT.ZDATAMIN) ZDATAMIN= ZDATA(NDATA) IF(ZDATA(NDATA).GT.ZDATAMAX) ZDATAMAX=ZDATA(NDATA) ndata=ndata+l

250 GOTO 200 300 CL0SE(UNIT=20)

WRITE(*,98)'XMIN= *.XDATAMIN,'XMAX='.XDATAMAX WRITE(*,98)'YMIN='.YDATAMIN,'YMAX='.YDATAMAX WRITE(*,98)'ZMIN=',ZDATAMIN,'ZMAX=',ZDATAMAX NDATA=NDATA-1 XMIN=XDATAMIN xMAX=xDATAMAX yMIN=yDATAMIN yMAX=yDATAMAX ZMIN=ZDATAMIN ZMAX=ZDATAMAX GOTO 310

C ****************** READ ALL DATA POINTS ******************* 301 OPEN(20,FILE=FNAME ,STATUS='OLD',ACCESS='SEQUENTIAL')

REWIND 20 NDATA=1

302 READ(20,FORMT ,END=303) XDATA(NDATA).YDATA(NDATA).ZDATA(NDATA) IF(XDATA(NDATA).EQ.0.0.OR.ZDATA(NDATA).EQ.0.0) goto 302

IF(XDATA(NDATA).LT.XDATAMIN) XDATAMIN=XDATA(NDATA) IF(XDATA(NDATA).GT.XDATAMAX) XDATAMAX=XDATA(NDATA) IF(YDATA(NDATA).LT.YDATAMIN) YDATAMIN=YDATA(NDATA) IF(YDATA(NDATA).GT.YDATAMAX) YDATAMAX=YDATA(NDATA) IF(ZDATA(NDATA).LT.ZDATAMIN) ZDATAMIN=ZDATA(NDATA) IF(ZDATA(NDATA).GT.ZDATAMAX) ZDATAMAX= ZDATA(NDATA) ndata=ndata+l GOTO 302

303 CLOSE(UNIT=20) NDATA=NDATA-1

WRITE(*,98)'XMIN='.XDATAMIN,'XMAX='.XDATAMAX WRITE(*,98)'YMIN='.YDATAMIN,'YMAX='.YDATAMAX

Appendix 6.3 (cont'd)

WRITE(*,98)'ZMIN= *,ZDATAMIN,'ZMAX= *.ZDATAMAX xMIN=XDATAMIN xMAX=xDATAMAX yMIN=yDATAMIN yMAX=yDATAMAX ZMIN=ZDATAMIN ZMAX=ZDATAMAX

310 WRITE(6,350)NDATA 350 FORMAT(IX,'NUMBER OF DATA P0INTS= ',15) 43 F0RMAT(1X,' WEST LIMIT OF DATA = ') 44 FORMATdX,' EAST LIMIT OF DATA = ') 45 FORMATdX,' SOUTH LIMIT OF DATA= ') 46 FORMAT(IX,' NORTH LIMIT OF DATA= ') 98 FORMAT(2X,A10,F10.2,10X,A10,F10.2)

RETURN END

C *************** SUBROUTINE FIT ************** SUBROUTINE FIT(FNAMEC,ndd.XDATA.YDATA,ZDATA,B) DOUBLE PRECISION XDATA(2000),YDATA(2000),ZDATA(2000),B

1,zsum,zs2,wsum,ws2 CHARACTER FNAMEC*17 OPEN(UNIT=l,FILE=FNAMEC,STATUS='unknown',ACCESS='SEQUENTIAL') ZSUH=O.0D+O0 ZS2=0.0D+00 WSUM=O.OD+00 WS2=0.0D+00 REWIND 1 1 = 1

10 READ(1,100,END=20)XDATA(I),YDATA(I),ZDATA(I),B ZSUM= ZSUM+ZDATA(I) ZS2= ZS2+ZDATA(I)*ZDATA(I) ZS3=ZSUM*ZSUM WSUM=WSUM+B WS2=WS2+B*B WS3=WSUM*WSUM 1 = 1+1 GO TO 10

20 CONTINUE CLOSE(UNIT=l)

100 FORMAT(2X.4F10.2) nn= i-1 SSR=WS2-(WS3/FLOAT(nn)) SST=ZS2-(ZS3/FLOAT(nn)) R2=SSR/SST Rr=SQRT(R2) £t=(r2/ndd)/((l-r2)/(nn-ndd-l)) print,' ' print,' ' print,'number of data =',nn print,'number of terms =',ndd PRINT , 'COEF.MULT.CORRELATION',Rr print,'significance test F =',ft RETURN END

Appendix 6.4 Computer program (Fortran-77L) RANDOM.

PROGRAM RANDOM C** COMPUTER PROGRAM TO RANDOMISE CLUSTERED DATA POINTS ************ C Written by: C C. N a s (Dept. of Geology, Univ. of Wollongong, Australia). C Last modification, January 1993. C This program splits map area with user defined retangular C block dimension. C One nearest point to the centre of each block is selected by C the program; coordinates and values from each randomised points C for variables being studied are stored in output file defined by C user. C ********************** KEY VARIABLES ****************************** C VARIABLE DESCRIPTION c

C X EASTING COORDINATE C Y NORTHING COORDINATE C GRADE COAL SEAM PARAMETER (ASH, SULFUR,THICKNESS, ETC) C WIDX WIDTH OF BLOCKS ALONG X AXIS C WIDY WIDTH OF BLOCKS ALONG Y AXIS C XIN INCREMENT OF X C YIN INCREMENT OF Y C XC EASTING COORDINATE OF CENTRE OF BLOCKS C YC NORTHING COORDINATE OF CENTRE OF BLOCKS C NX NUMBER OF GRIDS ALONG X-AXIS C NY NUMBER OF GRIDS ALONG Y-AXIS C FORMT FORMAT OF DATA FILE READ BY WINDOW C NHOL NUMBER OF DRILLHOLES C RANDOM.NML NAMELIST FILE CONTAINING DATAFILE NAME C *********************************************************************

COMMON/NAS1/HOLID(2500),Y(2500),X(2500),GRADE(2500) COMMON/OFF/XOF,YOF ,XSTl,YST1,XXW,XXE ,YYS,YYN,XW,XE,YS,YN,NX,NY NAMELIST/rnd/FNAME,FORMT,BLKDIM DATA MAXD.XMIN.YMIN,GRADEMIN/2500,9999999.,9999999., 999999./ DATA XMAX,YMAX,GRADEMAX/-9999999.,-999999.,-999999./ CHARACTER C*l,HOLID*10,FNAME*15,FORMT*50,FN*15

C ***************************************************************** PRINT,' THE PROGRAM REQUIRES TWO DATA FILES:* PRINT,' ' PRINT,' <1> RUN PARAMETERS IN random.nml FILE' PRINT,' <2> ASSAY DATA FILE ' PRINT,' ' PRINT,' enter X to exit OR ' PRINT, ' ANY KEY to continue > ' READ(*,5)C

5 FORMAT(Al) IF(C.EQ.'X'.OR.C.EQ.'x') STOP

C ***************************************************************** 0PEN(18,FILE='random.nml',STATUS='OLD') READ(18,rnd) PRINT,'WRITE OUTPUT FILE NAME ?',FN READ(*,*)FN OPEN(19,FILE=FN ,STATUS='UNKNOWN',ACCESS='SEQUENTIAL') OPEN(20,FILE=FNAME,STATUS='OLD*,ACCESS='SEQUENTIAL *)

C C READ DATA - CALL ROUTINE RDATA Q

CALL RDATA(FORMT,MAXD,NH0L,XMIN,XMAX,YMIN,YMAX.GRADEMIN.GRADEMAX) C

PRINT,'SEARCHING METH0D= retangle' CALL RETANG(NHOL,WIDX,WIDY,XIN,YIN) STOP END

C ******** SUBROUTINE RETANG TO SET RETANGLE BLOCKS ************* SUBROUTINE RETANG(NHOL,WIDX,WIDY,XIN,YIN)

C **************************************************************** DIMENSION XT(2500),YT(2500),ZT(2500) COMMON/NAS1/HOLID(2500),Y(2500),X(2500),GRADE(2500) COMMON/OFF/XOF ,YOF ,XST1 ,YST1 ,XXW ,XXE ,YYS ,YYN ,XW ,XE ,YS ,YN ,NX ,NY CHARACTER HOLID*10

C WRITE(6,5) READ(*,*)XW WRITE(6,6) READ(*,*)XE WRITE(6,7) READ(*,*)YS WRITE(6,8) READ(*,*)YN

5 FORMAT(IX,'WEST LIMIT OF GRID = ') 6 F0RMAT(1X,'EAST LIMIT OF GRID = ') 7 FORMAT(IX,'SOUTH LIMIT OF GRID= ') 8 FORMATdX,'NORTH LIMIT OF GRID= *) C **** INCREMENTS ****

Appendix 6.4 (cont'd)

WRITE(6,9) READ(*,*)WIDX WRITE(6,10) READ(*,*)WIDY

9 FORMAT(IX,*WIDTH OF BLOCKS ALONG X-AXIS= ') 10 FORMATdX,'WIDTH OF BLOCKS ALONG Y-AXIS= ') C

WRITE(6,11) READ(*,*)XIN WRITE(6,12) READ(*,*)YIN PRINT,' '

11 FORMAT(IX,'MOVING INCREMENTS ALONG X-AXIS= ') 12 FORMAT(IX,'MOVING INCREMENTS ALONG Y-AXIS= *)

nx =(XE-XW)/XIN ny =(YN-YS)/YIN PRINT, 'NUMBER OF GRID ALONG X-AXIS =',NX PRINT, 'NUMBER OF GRID ALONG Y-AXIS =',NY

C do 20 K = l,(ny) do 20 L = l,(nx) xl=XW+xin*(L-l) x2=xl-(widx/2) X3=Xl+(WIDX/2) yl=YS+yin*(K-l) y2=yl-(widy/2) Y3=Yl+(WIDY/2)

C C ***** SEARCHING DATA WITHIN EACH BLOCK ***** C

NDAT=1 DO 25 1=1,NHOL IF(X(i).LT.X2.0R.X(i).GT.X3) GOTO 25 IF(Y(i).LT.Y2.0R.Y(i).GT.Y3) GOTO 25 XT(NDAT) = X(i) YT(NDAT) = Y(i) ZT(NDAT) = GRADE(i) NDAT=NDAT+1

25 CONTINUE C

NDAT = NDAT-1 IF(NDAT.lt.l) go to 20

C ***** DISTANCE OF EACH POINT TO THE BLOCK CENTRE **** DIST = 0. DO 21 I = l.NDAT

D=(((XT(I)-X1)**2)+((YT(I)-Y1)**2))**0.5 IF (I.EQ.l) THEN

DIST = D NNP = 1

ELSE IF (D.LT.DIST) THEN

DIST = D NNP = I

ENDIF ENDIF

21 CONTINUE C ***** STORE RESULT TO A USER DEFINED OUTPUT FILE ***

WRITE (19,30)XT(NNP), YT(NNP), ZT(NNP) 20 CONTINUE 30 FORMAT (3F10.2)

RETURN END

C ********************* SUBROUTINE RDATA ***************************** SUBROUTINE RDATA(FORMT,MAXD,NHOL,XMIN,XMAX.YMIN,YMAX 1.GRADEMIN.GRADEMAX)

C**************************************************************** C THIS ROUTINE READS DATA AND DETERMINE MAXIMUM/MINIMUM COORD C****************************************************************

COMMON/NAS1/HOLID(2500),Y(2500),X(2500),GRADE(2500) COMMON/OFF/XOF,YOF,XST1,YST1,XXW,XXE,YYS,YYN,XW,XE,YS,YN,NX,NY CHARACTER HOLID*10,FORMT*50,C*1 PRINT,'LIMIT THE DATA BY THEIR CO-ORDINATES (Y/N)?: ' READ(*,10)C

10 FORMAT(Al) IF(C.EQ.'N'.OR.C.EQ.*n') GOTO 22

C ******* LIMIT DATA POINTS ****** WRITE(6,43) READ(5,*)XXW WRITE(6,44) READ(5,*)XXE WRITE(6,45) READ(5,*)YYS WRITE(6,46) READ(5,*)YYN

Appendix 6.4 (cont'd)

1=1 20 READ(20,FORMT,END=21) X(I) ,Y(I),GRADE(I) C C ZERO GRADE k COORDINATES ARE ASSUMED TO BE BLANK LINE C

IF(X(I).EQ.0.0.OR.GRADE(I).EQ.0.0) GO TO 20 IF(X(I).LT.XXW.OR.X(I).GT.XXE)GO TO 20 IF(Y(I).LT.YYS.OR.Y(I).GT.YYN)GO TO 20 IF(X(I).LT.XMIN) XMIN=X(I) IF(X(I).GT.XMAX) XMAX=X(I) IF(Y(I).LT.YMIN) YMIN=Y(I) IF(Y(I).GT.YMAX) YMAX=Y(I) IF(GRADE(I).LT.GRADEMIN) GRADEMIN = GRADE(I) IF(GRADE(I).GT.GRADEMAX) GRADEMAX=GRADE(I) 1 = 1+1 IF(I.LE.MAXD) GO TO 20 PRINT,'** DATA ALLOWED EXCEEDED - ONLY FIRST *,MAXD,' USED'

21 CONTINUE GO TO 40

C****** READ ALL DATA ********** 22 1 = 1 23 READ(20,FORMT,END=24) X(I),Y(I),GRADE(I)

IF(X(I).EQ.0.0.OR.GRADE(I).EQ.0.0) GO TO 23 IF(X(I).LT.XMIN) XMIN=X(I) IF(X(I).GT.XMAX) XMAX=X(I) IF(Y(I).LT.YMIN) YMIN=Y(I) IF(Y(I).GT.YMAX) YMAX=Y(I) IF(GRADE(I).LT.GRADEMIN) GRADEMIN=GRADE(I) IF(GRADEd)-GT.GRADEMAX) GRADEMAX=GRADE(I) 1 = 1+1 IF(I.LE.MAXD) GO TO 23 PRINT,'** DATA ALLOWED EXCEEDED - ONLY FIRST '.MAXD,' USED'

24 CONTINUE C 40 NHOL=I-l C C DEBUG STATEMENTS C

PRINT,'NUMBER OF DATA POINTS=',NHOL PRINT,'XMIN=',XMIN , 'XMAX=',XMAX PRINT , *YMIN= ' ,YMIN , *YMAX= * ,YMAX PRINT,'VALUE MIN='.GRADEMIN,'VALUE MAX='.GRADEMAX PRINT,' '

43 FORMAT(IX,' WEST LIMIT OF DATA = ') 44 FORMAT(IX,' EAST LIMIT OF DATA = ') 45 FORMATdX,' SOUTH LIMIT OF DATA= *) 46 FORMAT(IX,' NORTH LIMIT OF DATA= ') C

RETURN END

Appendix 6.5 Drill hole data for the Sangatta seam.

DDH

C2061 C2063 C2089 C2246 C2264 C2271 C22S2 C2290 C2320 C2329 C2331 C2332 C2334 C2341 C2343 C2442 C2517 C2518 C2519 C2521 C2S22 C2552 C2553 C2554 C255S C25S6 C2579 C2585 C2635 C2643 C2644 C2645 C2646 C2670 C2693 C2694 C269S C2696 C2810 C2811 C2812 C2866 C2867 C2868 C28S9 C291S C2916 C29I7 C2918 C2919 C2920 C2921 C2922 C2923 C2924 C292S C2926 C2942 C2982 C2983 C2984 C298S C2986 C2994 C2995 C2996 C2999 C3000 C3001 C3002 C3003 C3004 C30O5 C3006 C3007 C3015 C3016 C3017 C3018 C3019 C3020 C3021 C3022 C3029 C3030 C3031 C3032 C3037 C3038

C3039 C3040 C3041 C3042 C30S1 C3141 C3143 C3145 C3146 C3147 C31S0 C3151 C31S2 C31S3 C3154 C3156 C31S7 C31S8 C31S9 C3230 C3231 C3233 C3234 C3236 C3237 C3368 C336S C3370 C3391 C3392 C3393 C3394 C339S C3396 C3397 C3399 C3400 C3401 C3405 C3409 C3410 C3411 C3412 C3413 C3443 C3444 C3445

EASTING tn)

99090.20 99429.40 98776.40 98788.70 99086.46 99910.38 97370.20 98712.31 98873.24 98904.90 96330.61 9S71S.63 98519.88 97216.58 98388.37 97689.39 98835.53 98221.68 97739.81 97612.29 97661.33 96514.24 96296.45 96074.91 96831.13 97102.74 96110.64 98058.92 98722.02 97767.75 98080.00 97415.57 98728.14 98544.59 99111.17 99105.11 98986.89 98950.65 99060.52 99029.85 99036.07 99087.73 99075.28 99085.10 99071.06 98777.81 98726.09 984 69.41 98506.21 98532.18 98360.91 98431.88 98194.13 98380.44 98725.57 98450.71 99016.59 101239.44 96488.47 96463.11 96182.38 96605.49 96880.09 99145.32 98990.72 99047.45 97218.31 96615.93 96277.19 96735.64 96399.95 96675.24 96806.03 96966.24 96966.18 97829.75 98015.11 98389.35 98129.82 97580.88 97740.95 97760.92 98021.30 97224.10 99097.30 97651.76 97926.21 97457.62 97391.71 97181.80 97464.08 97513.03 97063.44 98327.73 98930.95 98794.71 98509.85 98602.85 98603.07 98661.34 98838.15 98607.12 98714.75 98371.54 98382.61 98364.93 98562.94 99020.05 98811.34 98758.27 98906,30 98752.25 98823.58 98759.49 100025.38 100012.55 99584.35 99187.70 99215.15 99294.58 99295.60 99265.07 99131.79 99168.54 98644.70 99505.51 97613.91 99014.01 99004.14 97617.33 97617.91 97616.35 97613.43 99916.22 100025.77 99260.97

NORTHING

(•) 201766.50 201141.50 197896.91 195847.50 198701.20 204130.00 195055.59 194932.09 195054.50 200228.41 195022.41 195565.30 195243.70 195589.27 197435.88 196985.42 195505.30 194515.27 194243.47 194761.20 195438.36 195987.34 194759.31 195750.89 195233.52 194754.34 195500.66 195009.44 198249.95 194501.39 194755.25 196245.17 198581.69 195956.77 195404.17 195294.34 195355.97 195841.73 195293.38 195272.63 195328.05 195317.09 195311.45 195305.38 195299.06 195251.09 195366.94 195373.88 195625.16 195766.11 195741.59 195880.97 195519.44 195128.30 195124.61 195001.56 195503.36 195215.77 194598.25 194871.38 195125.97 195046.09 194750.64 195339.09 195434.44 195453.83 195262.02 195245.95 195457.41 195382.25 195752.13 195742.27 195761.20 195487.09 195359.56 194311.34 194496.70 194517.13 194619.98 194497.94 194775.72 195013.95 194867.52 195376.27 195322.64 195194.00 195242.91 195272.78 194879.55 195127.02 195498.22 195746.91 195746.13 194756.95 195250.02 195004.84 195120.03 195133.48 195130.44 195258.56 195377.23 195378.94 195503.20 195388.59 195504.95 195258.38 195024.02 195070.98 195181.59 195447.16 195454.09 195065.86 195301.41 195066.84 203808.63 204475.77 203490.88 202491.70 202249.98 202020.34 202023.05 201483.06 201020.63 200526.55 200254.97 203237.34 195127.88 195755.89 195767.42 195127.55 195129.94 195131.64 195132.42 203758.02 204219.38 203019.08

COLLAR In)

142.02 192.90 143.56 125.15 177.31 146.74 114.56 133.14 90.68 163.28 159.04 107.14 85.12 93.45 166.67 160.20 138.32 114.50 82.61 94.89 138.70 97.04 128.04 68.01 71.65 39.50 120.24 61.24 171.70 136.56 95.72 131.50 147.30 88.30 146.18 136.18 127.43 134.03 126.01 121.68 128.52 132.05 131.70 131.65 130.84 110.93 113.38 75.27 82.69 81.76 64.02 78.48 48.31 58.45 76.92 44.49 153.49 71.74 130.48 143.99 152.16 100.89 75.90 145.12 139.12 151.61 51.00 92.07 150.38 67.66 134.22 94.85 77.96 48.60 45.04 104.15 127.08 85.09 109.62 92.71 127.13 143.20 102.12 82.63 134.18 154.46 68.07 105.84 61.88 49.33 106.30 124.21 73.13 40.75 113.14 74.99 55.94 60.52 60.40 99.38 125.72 105.22 126.91 64.89 67.81 50.96 47.91 87.30 101.41 131.74 152.84 66.81 119.62 67.05 193.76 85.62 139.77 80.40 107.49 114.28 114.32 177.93 152.23 192.87 137.28 141.86 145.10 159.53 156.25 145.65 145.75 145.79 145.25 208.96 119.21 111.64

DEPTOP (ml

67.65 30.73 46.21 33.59 51.52 67.06 122.38 80.61 32.49 71.86 73.87 92.65 45.72 106.49 141.40 200.86 35.09 108.74 110.65 98.15 135.34 154.27 43.27 29.55 37.97 36.42 35.20 62.59 103.54 125.29 102.65 179.03 79.78 26.27 13.64 7.78 15.41 11.14 6.56 10.65 10.02 3.41 6.72 4.93 8.63 50.53 44.26 35.42 28.66 26.64 35.17 37.73 30.63 27.80 15.00 19.66 18.50 59.39 31.32 71.34 57.78 54.15 26.48 0.30 19.26 17.50 46.19 50.92 84.04 33.28 144.34 115.67 96.19 41.70 27.24 91.50 126.04 76.28 111.06 53.73 129.70 135.82 112.63 86.54 2.79 166.32 60.74 109.79 63.87 52.72 125.86 138.15 98.74 27.88 29.06 29.50 28.67 25.64 28.32 47.72 39.17 49.21 41.84 48.02 38.03 11.84 15.16 22.01 28.75 38.34 47.96 7.21 47.62 7.89 72.45 28.55 112.22 4.89 29.19 12.20 11.90 61.44 58.60 58.35 103.83 123.64 136.41 31.82 26.62 137.12 141.88 141.34 139.98 112.85 27.16 134.84

DEPBOT (ml 76.93 37.06 51.25 40.16 58.72 73.41 130.30 89.30 38.08 76.84 80.36 100.14 53.09 111.09 149.47 207.64 44.07 113.60 118.85 108.68 139.60 162.37 49.67 34.25 49.33 42.76 40.26 68.28 110.00 133.95 110.32 190.32 85.22 34.24 18.12 14.18 26.72 18.09 14.06 18.69 18.43 11.37 14.39 12.59 15.95 60.58 51.70 40.91 37.26 36.27 40.77 44.87 37.62 33.35 19.38 25.58 25.33 62.66 39.31 78.07 64.42 63.68 32.74 9.50 27.05 24.20 52.90 61.40 98.14 45.78 149.91 126.44 102.24 45.87 37.18 97.25 133.36 82.12 121.28 61.17 140.81 139.04 120.01 96.45 11.64 173.25 63.38 121.32 71.20 58.73 132.87 142.29 104.07 34.27 33.85 35.49 35.44 34.52 35.02 53.99 47.14 51.61 46.08 55.15 45.93 15.08 20.86 29.33 32.09 45.26 55.60 12.47 56.01 13.08 77.17 32.06 118.19 12.30 38.24 22.72 22.36 67.70 64.74 66.46 113.55 129.91 141.71 34.17 31.30 142.22 144.10 146.95 143.36 117.83 29.30 140.82

THICK Id) 6.89 6.33 5.04 6.57 7.20 6.35 7.92 8.69 5.59 4.98 6.49 7.49 7.37 4.60 8.07 6.78 8.40 4.86 8.20 10.53 4.26 8.10 6.40 4.70 11.36 6.34 5.06 5.69 6.46 8.67 7.67 11.29 5.44 7.97 4.48 6.40 10.91 6.95 7.50 6.04 B.41 7.96 7.67 7.65 7.32 10.05 7.44 5.49 8.60 9.63 5.60 7.14 6.99 5.55 4.38 5.92 S.83 3.27 7.99 6.73 6.64 9.53 6.26 9.20 7.79 6.70 6.71 10.48 4.10 12.50 5.57 10.77 5.05 3.59 9.94 5.75 6.34 5.84 10.22 7.44

11.11 3.22 7.38 9.45 8.42 S.93 2.64 10.49 7.33 6.01 7.01 4.14 5.33 6.39 4.79 5.99 6.77 8.88 6.70 6.27 7.97 2.40 4.24 7.13 7.90 3.24 S.70 7.32 3.34 6.92 7.64 5.26 8.39 5.19 4.72 3.51 5.97 7.41 9.05 10.52 10.46 6.26 6.14 8.11 9.72 6.27 5.30 2.35 4.68 4.70 2.22 5.09 3.48 4.98 2.14 5 .98

TOPELEV Iml

74.37 162.17 97.35 91.56 125.79 79.68 -7.82 52.53 58.19 91.42 B5.17 14.49 39.40 -13.04 25.27 -40.66 103.23 5.76 -28.04 -3.26 3.36 -57.23 84.77 38.46 33.68 3.08 85.04 -1.35 68.16 11.28 -6.93 -47.53 67.52 62.03 132.54 128.40 112.02 122.89 119.45 111.03 118.50 128.64 124.98 126.72 122.21 60.40 69.12 39.85 54.03 55.12 28.85 40.75 17.68 30.65 61.92 24.83 134.99 12.35 99.16 72.65 94.38 16.74 49.42 144.92 119.86 134.11 4.81 41.15 66.34 34.38 -10.12 -20.82 -18.23 6.90 17.80 12.65 1.04 8.81 -1.44 38.98 -2.57 7.38 -10.51 -3.91 131.39 -11.86 7.33 -3.95 -1.99 -3.39 -19.56 -13.94 -25.61 12.87 84.08 45.49 27.27 34.88 32.08 51.66 86.55 56.01 85.07 36.87 29.78 39.12 32.75 65.29 72.66 93.40 104.88 59.60 72.00 59.16 121.31 57.07 27.55 75.51 78.30 102.08 102.42 116.49 93.63 134.52 33.45 18.22 8.69 127.71 129.63 3.53 3.87 4.45 5.37 96.11 92.05 -23.20

BOTE LEV

Iml 65.09 155.84 92.31 84.99 118.59 73,33 -15.74 43,84 52.60 86.44 78.68 7.00 32.03 -17.64 17.20 -47.44 94.25 0.90 -36.24 -13.79 -0.90 -65.33 78.37 33.76 22.32 -3.26 79.98 -7.04 61.70 2.61 -14.60 -58.82 62.08 54.06 123.06 122.00 100.71 115.94 111.95 102.99 110.09 120.68 117.31 119.07 114.89 50.35 61.68 34.36 45.43 45.49 23.25 33.61 10.69 25.10 57.54 18.91 128.16 9.08 91.17 65.92 87.74 37.21 43.16 135.62 112.07 127.41 -1.90 30.67 62.24 21.88 -15.69 -31.59 -24.28 2.73 7.86 6.90 -6.28 2.97 -11.66 31.54 -13.68 4.16 -17.89 -13.82 122.54 -18.79 4.69 -15.48 -9.32 -9.40 -26.57 -18.08 -30.94 6.48 79.29 39.50 20.50 26.00 25.38 45.39 78.58 53.61 80.83 29.74 21.88 35.88 27.05 57.97 69.32 86.48 97.24 54.34 63.61 53.97 116.59 53.56 21.58 69.10 69.25 91.56 91.96 110.23 B7.49 126.41 23.73 11.95 3.39 125.36 124.95 3.43 1.65 -1.16 1.89 91.13 B9.91 -29.18

DDH

C3449 C3451 C3454 C3482 C3484 C3486 C3491 C3492 C3493 C3495 C3496 C3500 C3502 C3507 C3511 C3521 C3536 C3538 C3539 C3575 C3576 C3631 C3634 C3635 C3637 C3641 C3699 C3700 C3701 C3702 C3704 C3706 C3756 C3758 C3882 C3884 C3885 C3887 C3897 C3909 C3941 C4042 C4239 C5123 C5369 C5370 C5482 C5483 C5484 C5485 C5486 C5487 C5488 C5565 C5570 C6243 C6244 C6246 C6255 C6257 C6260 C69S3 C6954 C6955 C7052 C7102 C7652 C7659 R2001 R2002 R2009 R2010 R2018 R2023 R2033 R2035 R2037 R2042 R2044 R2047 R2053 R2054 R20 56 R2072 R2077 R2079 R2080 R2098 R2104 R210S R2112 R2114 R2121 R2126 R2127 R2145 R2147 R2179 R2189 R2190 R2191 R2192 R2202 R2204 R2208 R2209 R2213 R2234 R2236 R2237 R2238 R2241 R2243 R2244 R2245 S2247 R2248 R2253 R2254 R2258 R2259 R2263 R2265 R2267 R2268 R2270 R2276 R2280 R2281 R2283 R2316 R2317 R2319 R2325 R2345 R2353

EASTING In)

98520.40 98380.51 98763.63 96494.19 96632.53 96239.91 96364.22 96599.69 96836.06 96921.30 96848.11 96882.57 96241.08 98732.33 98351.69 98349.19 97599.90 98226.95 97655.50 99089.38 99109.86 98019.06 97914.93 97751.18 98228.17 97652.57 96216.27 96389.63 96388.76 96385.94 96258.81 96811.46 98819.23 9883S.S1 98561.81 98669.43 98669.85 98611.68 98946.43 98544.97 99032.48 99157.88 97574.56 96534.09 98105.34 98023.44 98077.79 98084.42 97939.83 97993.16 98024.08 98023.24 97934.81 98204.55 98092.68 99176.55 99002.08 99004.77 99001.66 98857.61 97007.27 99112.75 99107.03 99106.14 93854.69 94478.18 100706.96 100483.93 99840.48 99601.89 99170.49 98705.33 98311.07 98965.73 92862.18 96112.10 97759.92 98458.05 94929.20 98594.60 100373.20 100027.90 99681.60 98618.10 98904.30 98131.50 98776.70 94574.74 100874.60 100880.50 98575.40 99004.36 96325.96 99996.26 101176.00 101553.35 101082.50 99061.30 101365.80 100577.60 99876.42 99909.23 100324.20 99142.99 96715.10 96277.30 98788.30 99192.40 97862.70 97661.20 97611.90 96720.30 97220.00 97365.46 98412.40 984 49.72 98533.36 98873.40 98388.40 98583.90 98715.50 99087.20 99070.90 99453.90 99075.29 99246.52 96715.76 99844.20 99765.69 97831.63 100277.80 100481.40 99505.59 99572.52 98870.80 96585.42

NORTH INS (m)

200570.17 200008.55 199768.66 194680.16 194759.00 194822.64 195122.16 194882.08 194875.41 195039.64 195122.06 194751.27 194904.16 195314.31 195630.19 195633.20 194610.20 194619.80 194332.45 198841.56 198448.05 194863.55 194628.83 194901.69 194612.61 194325.77 195257.48 19533S.47 195336.97 195335.72 195625.95 195490.80 195183.00 195249.16 195263.45 195434.08 195433.20 195332.97 195047.45 195317.86 198621.30 198538.25 194474.94 195123.75 195709.25 195929.80 196053.53 195820.67 195741.05 195595.73 193313.23 195318.27 195741.92 194804.55 194366.72 199144.34 199189.47 199183.25 199073.91 199033.94 194749.84 195267.55 195267.55 195272.64 198080.56 196901.44 194491.39 194495.47 203828.06 202805.50 200530.70 200573.50 198419.80 199465.50 199591.20 195168.50 195011.80 197136.00 197072.41 201738.59 204931.00 203808.70 203369.20 198421.80 200225.00 196659.09 197901.50 196787.30 194549.20 194157.09 195486.27 196438.91 195023.91 204920.67 205478.63 205130.41 205155.50 199333.41 205859.70 205317.50 204616.41 204133.30 205188.20 198563.41 194929.80 195459.09 195851.91 195332.09 194739.41 195440.70 196330.30 195565.20 195589.09 195053.20 195992.80 195200.41 195243.91 195057.70 197437.70 198068.00 198712.70 198704.50 201179.50 202247.70 202056.00 202837.00 193594.30 194782.70 195144.00 194311.00 195039.70 194609.20 194890.80 199456.30 201754.81 194299.77

COLLAR (ml

121.57 94.36 124.53 111.65 103.77 111.27 135.61 139.89 106.18 84.76 87.37 76.01 113.51 109.90 62.02 61.75 82.60 88.57 93.88 158.91 178.99 102.24 172.80 132.74 38.32 93.27 134.53 107.87 107.94 107.78 126.63 78.39 101.01 109.14 92.64 117.83 117.86 99.96 83.04 86.32 173.56 195.67 92.88 124.95 30.47 53.43 40.68 39.90 56.30 32.83 27.89 27.96 56.60 57.31 B9.38 146.67 135.87 135.75 121.43 119.29 42.44 127.70 127.74 127.91 46.60 80.49 19.24 17.58 181.81 130.54 192.75 145.55 133.09 181.73 72.75 152.76 143.21 159.40 100.73 104.30 132.40 193.85 170.90 174.75 163.07 170.50 143.70 102.94 43.97 40.48 99.32 196.71 159.11 114.23 131.50 130.97 159.40 160.12 91.34 101.18 135.42 146.63 99.96 197.29 132.98 150.19 124.82 152.23 162.25 138.60 160.79 107.09 93.60 114.14 74.62 78.74 85.17 90.80 166.83 128.61 130.23 177.30 148.60 164.29 109.11 95.91 91.38 78.51 92.13 104.26 73.73 18.82 37.16 218.01 150.47 142.55

DEPTOP (•)

134.62 109.50 98.91 46.02 42.88 19.51 60.58 80.79 57.70 42.40 45.02 26.34 20.82 46.21 21.55 22.70 72.13 83.92 58.62 34.22 38.03 112.82 177.65 140.55 83.75 58.20 47.41 39.15 39.10 38.93 76.58 56.66 32.10 41.72 48.67 49.21 48.97 48.72 22.20 43.20 55.00 51.53 51.70 71.94 11.14 37.56 10.84 18.82 51.61 33.83 33.46 34.11 56.52 55.99 107.32 23.42 37.82 36.84 13.97 38.71 9.00 3.64 5.47 3.60 47.42 34.00 34.80 47.48 106.33 50.93 57.50 115.50 147.86 98.68 183.52 54.54 134.06 99.69 150.79 167.96 61.80 71.57 113.84 135.41 70.98 145.47 46.78 68.50 25.67 104.29 32.29 73.45 73.64 131.75 92.10 34.10 59.44 55.94 103.05 135.98 132.34 67.50 85.58 58.00 80.22 83.88 33.21 20.50 173.97 134.90 191.08 92.39 105.78 121.63 34.66 44.00 45.28 32.18 141.97 83.37 63.77 51.36 83,90 52.90 51.87 109.60 135.77 126.45 61.36 90.92 4.56 26.96 82.20 11.25 131.72 25.12

DEPBOT In) 141.51 121.26 104.73 52.21 49.96 25.83 67.47 87.94 62.91 49.02 56.03 32.18 27.12 53.26 25.37 32.72 79.84 91.60 64.06 40.73 44.67 120.13 186.50 147.55 91.75 63.55 54.18 46.35 46.33 46.10 84.80 68.12 33.46 48.25 54.24 49.90 55.64 52.18 29.45 46.10 62.85 58.72 59.45 81.93 19.04 42.95 15.88 26.17 63.35 41.48 41.08 42.02 65.14 62.54 115.83 29.56 44.02 73.36 17.87 41.15 9.94 5.30 6.71 8.50 47.88 35.45 38.31 49.75 111.19 57.12 65.92 121.88 157.00 100.38 187.36 57.53 137.10 102.70 152.23 175.95 64.43 76.79 118.65 142.47 75.61 149.36 51.94 69.96 26.86 105.18 34.56 79.97 80.11 135.00 96.17 44.83 63.03 60.67 106.95 139.35 135.72 74.01 89.94 65.00 88.65 88.03 39,95 21.10 184.32 139.08 201.34 101.48 111.50 129.33 37.21 47.00 52.50 37.88 149.77 90.32 65.36 58.44 90.86 54.15 62.21 116.16 140.30 127.98 62.98 97.03 6.14 28.91 B4.06 12.65 135.62 27.07

THICK On) 6.89 11.76 5.B2 6.19 7.08 6.32 6.89 7.15 5.21 5.97 11.01 5.84 6.30 7.05 3.82 10.02 7.71 7.68 5.44 5.83 6.64 7.31 8.85 7.00 8.00 5.35 6.77 7.20 7.23 7.17 7.63 10.55 1.36 6.53 5.57 0.69 4.55 3.46 7.25 2.90 7.85 7.19 7.75 9.99 7.90 5.39 3.99 7.35 11.23 7.65 7.62 7.72 5.44 6.55 8.51 6.14 6.20 8.80 3.90 2.44 0.94 1.66 2.14 4.90 0.46 1.45 1.35 2.27 4.96 6.19 8.42 6.38 9.14 1.70 4.34 2.99 3.04 2.66 1.44 7.99 2.63 5.22 4.81 7.06 4.63 3.89 5.16 1.46 1.19 0.89 2.27 6.52 6.47 3.25 4.07 10.73 3.59 4.73 3.90 3.37 3.38 6.51 4.36 7.00 8.43 4.IS 6.74 0.60 10.35 4.18 10.26 9.09 5.72 7.70 2.55 3.00 7.22 5.70 7.80 6.95 1.59 7.08 6.96 1.25 9.87 6.56 4.53 1.53 1.62 6.11 1.58 1.95 1.86 1.40 3.90 1.95

TOPELEV In)

-13.05 -15.14 25.62 65.63 60.89 91.76 75.03 59.10 48.48 42.36 42.35 49.67 92.69 63.69 40.47 39.05 10.47 4.65 35.26 124.69 140.96 -10.58 -4.85 -7.81 4.57 35.07 87.12 68.72 68.84 68.85 50.05 21.73 68.91 67.42 43.97 68.62 68.89 51.24 60.84 43.12 118.56 144.14 41.18 53.01 19.33 15.87 29.84 21.09 4.69 -1.00 -5.57 -6.15 0.08 1.32 -17.94 123.25 98.05 98.91 107.46 80.58 33.44 124.06 122.27 124.31 -0.82 46.49 -15.56 -29.90 75.48 79.61 135.25 30.05 -14.77 93.05 -110.7 98.22 9.15 59.71 -50.06 -63.66 70.60 122.28 57.06 39.34 92.09 25.03 96.92 34.44 18.30 -63.81 67.03 123.26 85.47 -17.52 39.40 96.87 99.96 104.28 -11.71 -34.80 3.08 79.13 14.38 139.29 52.76 66.31 91.61 131.73 -11.72 3.70 -30.29 14.70 -12.18 -7.49 39.96 34.74 39.89 58.62 24.86 45.24 66.46 125.94 64.70 111.39 57.24 -13.69 -44.39 -47.94 30.77 13.34 69.17 -8.14 -45.04 206.76 18.75 117.43

BOTELEV tin)

-19.94 -26.90 19.80 59.44 53.81 85.44 68.14 51.95 43.27 35.74 31.34 43.83 86.39 56.64 36.65 29.03 2.76 -3.03 29.82 118.18 134.32 -17.89 -13.70 -14.81 -3.43 29.72 80.35 61.52 61.61 61.68 41.83 10.27 67.55 60.89 38.40 67.93 62.22 47.78 53.59 40.22 110.71 136.95 .33.43 43.02 11.43 10.48 24.80 13.73 -7.OS -8.65 -13.19 -14.06 -8.54 -5.23 -26.45 117.11 91.85 62.39 103.56 78.14 32.50 122.40 119.03 119.41 -1.28 45.04 -19.07 -32.17 70.62 73.42 126.83 23.67 -23.91 81.35 -115.11 95.23 6.11 56.70 -51.50 -71.65 67.97 117.06 52.25 32.28 87.46 21.14 91.76 32.98 17.11 -64.70 64.76 116.74 79.00 -20.77 35.33 86.14 96.37 99.45 -15.61 -38.17 -0.30 72.62 10.02 132.29 44.33 62.16 84.87 131.13 -22.07 -0.48 -40.55 5.61 -17.90 -15.19 37.41 31.74 32.67 52.92 17.06 38.29 64.87 118.86 57.74 110.14 46.90 -20.25 -48.92 -49.47 29.15 7.23 67.59 -10.09 -46.90 205.36 14.85 115.48

Appendix 6.5 (confd)

DDH

R2354 R2357 R2358 R23S9 R2370 R2372 R2373 R2374 R2375 R2377 R2378 R2379 R2380 R2381 R2383 R2384 R2386 R2387 R2388 R2389 R2391 R2392 R2393 R2399 R2400 R2401 R2402 R2403 R2404 R2405 R2406 R2407 R2410 R2411 R2417 R2418 R2419 R2420 R2421 R2422 R2423 R2424 R2425 R2426 R2428 R2429 R2432 R2433 R2434 R2435 R2436 R2437 R2441 R2443 R2447 R2448 R2449 R2456 R2457 R2458 R2460 R2461 R2462 R2463 R2464 R2465 R2466 R2467 R2470 R2483 R2485 R2486 R2488 R2490 R2491 R2492 R2495 R2498 R2500 R2S01 R2S03 R2S04 R2507 R2520 R2525 R2527 R2528 R2529 R2530 R2531 R2532 R2533 R253S R2536 R2537 R2S38 R2539 R2540 R2541 R2542 R25S0 R2557 R2559 R2S63 R2564 R2565 R2566 R2567 R2568 R2569 R2570 R2581 R2582 R2583 R2584 R2586 R2587 R2588 R2634 R2636 R2638 R2648 R2657 R2658 R2661 R2662 R2663 R2679 R2680 R2681 R2682 R2686 R2687 R2688 R2689 R2690

EASTING (m)

95532.51 98481.17 98817.64 99106.87 98932.21 98361.50 98836.43 98777.99 98994.44 98194.47 99017.85 97334.05 97155.91 97074.84 97586.44 97584.81 98055.14 97981.43 97935.48 97463.58 97061.21 97338.73 98104.76 96547.77 96804.86 96272.44 96503.90 96967.43 96109.21 97748.98 97998.44 98256.43 95736.54 95408.92 96393.59 96608.69 96831.44 96948.22 96296.52 96577.03 96806.13 97102.76 96546.74 97018.06 96074.42 97691.27 97298.48 96403.55 96434.72 95290.57 97439.28 96978.01 96109.80 95162.67 97848.33 97511.73 97524.44 97816.52 97613.15 97768.68 98014.24 98223.70 98079.95 98328.37 98573.55 98507.42 98469.53 98362.46 98069.41 97739.91 97756.00 97211.74 96503.39 96217.12 96394.49 95329.76 95842.37 96213.69 97830.72 98058.35 98167.01 97459.10 98391.21 97578.66 98597.00 97553.38 97573.46 96403.48 96931.22 98092.89 97986.31 98318.29 98070.88 99008.97 99279.55 98475.65 98722.23 98964.90 98873.37 94934.81 98542.01 96948.76 97057.33 99742.68 99321.18 99227.30 99468.08 99261.70 98762.55 98909.19 98824.23 98911.56 98728.29 99007.57 98871.24 95871.75 96803.77 96735.46 98217.15 99172.81 94465.12 98870.41 98950.81 98860.33 98740.05 98664.25 98549.01 97788.65 97906.46 99108.48 99103.48 98990.96 98985.17 98917.31 99008.44 98882.96

NORTHING (ml

193718.59 199436.59 198453.98 198448.66 195749.98 195743.03 195500.55 195248.67 195259.27 195517.03 195503.38 194761.09 194998.28 195233.48 194987.59 195257.09 195008.27 195228.94 195495.33 195500.34 195746.52 195761.77 195749.17 195747.16 195759.70 195751.67 195503.91 195486.13 195500.66 196498.70 196500.58 196502.19 195992.08 196244.52 195263.91 195240.09 195235.63 195006.39 194756.73 194754.98 1947S7.33 194751.33 195006.27 194476.45 195752.59 196989.86 197747.61 197000.64 196749.89 197746.45 197000.72 197003.08 196015.52 196752.20 195273.42 195748.95 195990.02 196261.97 194757.69 194499.48 194499.06 194511.91 194757.81 194754.66 195872.78 195625.92 195376.11 195255.81 196242.88 194246.50 195508.81 195238.19 195899.41 195261.13 196000.63 196499.19 195997.41 194752.41 196492.39 196504.70 195001.09 195272.34 194516.31 194498.22 197253.41 196495.84 196734.23 196243.41 195987.41 197509.52 197746.38 197253.58 196985.66 198993.00 199000.59 198256.55 198247.00 198251.23 197997.48 197759.59 197747.77 194761.30 195004.73 199001.81 199258.20 199496.09 199495.19 199758.34 199771.59 198749.67 198270.98 198602.03 198583.44 199751.14 199252.20 196257.95 195047.4S 195380.63 198249.44 198739.05 197752.20 199593.31 195839.00 195857.55 195939.52 195961.98 195956.84 194861.19 194992.50 195406.55 195296.63 195432.44 195358.91 194997.34 195085.81 195613.06

COLLAR (ml

28.14 136.38 186.04 179.18 144.80 63.92 138.27 111.01 119.00 48.29 153.52 42.31 28.05 39.55 117.79 135.67 61.61 59.23 63.45 106.40 73.24 96.55 34.99 106.94 78.18 116.60 129.06 48.40 120.09 121.46 131.08 134.69 56.85 81.68 113.98 90.07 71.56 85.34 127.61 107.96 89.94 39.52 138.16 95.47 67.96 160.09 112.68 110.25 132.32 38.02 170.16 104.43 120.38 65.18 97.14 124.22 159.15 97.79 94.87 136.60 127.02 114.07 95.79 40.77 93.60 82.73 75.54 49.96 53.12 82.60 110.66 58.50 100.24 134.47 106.54 55.41 71.39 111.07 121.42 142.54 35.56 106.00 85.17 92.56 93.93 184.00 195.38 112.18 74.83 172.60 152.44 159.44 197.19 131.98 148.48 143.64 171.70 144.34 156.93 59.01 86.41 70.86 50.24 119.63 163.27 173.41 197.30 156.25 124.49 143.38 189.26 162.42 147.27 155.52 161.51 6 4.87 100.77 67.37 120.73 168.27 51.38 147.67 134.20 124.30 112.41 100.55 88.31 151.73 107.08 146.11 136.11 138.92 127.56 78.26 90.58 164.31

DEPTOP DEPBOT THICK TOPELEV BOTELEV (m)

13.85 123.09 97.27 39.70 37.46 34.95 36.27 50.52 17.25 30.83 18.64 31.53 27.04 19.50 110.75 134.52 63.03 40.12 46.08 125.50 98.60 120.80 14.17 117.32 95.83 106.05 84.12 11.42 30.87 137.03 116.42 109.13 71.09 74.05 45.95 50.81 38.08 40.72 43.06 45.22 42.14 35.80 81.46 37.89 29.64 200.45 231.33 241.76 224.07 200.74 228.40 203.65 184.76 108.80 91.44 137.38 176.24 104.23 98.05 125.86 115.97 108.35 103.31 27.84 29.47 29.90 35.77 10.71 18.30 99.84 95.10 56.08 148.67 48.09 169.21 102.48 98.16 17.81 132.61 117.50 27.40 109.97 76.01 53.24 26.80 228.37 234.11 183.71 119.43 194.50 183.50 139.25 190.98 27.95 2.62 125.36 103.10 17.01 48.98 190.04 43.52 27.15 34.55 64.13 9.79 26.19 2.00 11.23 98.68 47.91 100.40 58.63 79.77 80.09 96.22 138.06 54.09 32.92 138.88 27.66 116.85 94.66 11.53 20.55 29.21 21.65 26.03 161.38 111.30 12.84 7.72 19.30 15.23 29.31 25.30 42.20

(ml 19.10 131.19 104.32 47.18 38.87 39.97 46.34 60.60 24.86 38.05 24.84 40.36 34.29 26.20 113.92 146.95 68.71 42.20 47.90 132.28 104.86 123.39 20.74 131.60 101.73 110.67 91.81 15.46 39.81 141.16 123.44 115.37 73.12 74.66 53.02 ' 61.17 48.73 46.31 19.56 52.07 52.35 42.29 88.78 38.82 34.59 207.02 238.08 250.17 226.38 202.67 237.09 210.72 185.32 110.27 110.56 141.38 181.05 109.83 108.25 133.92 132.03 113.01 110.93 34.79 35.72 37.72 11.50 13.70 19.50 108.32 96.88 62.78 162.89 54.92 178.77 104.58 103.14 24.52 134.02 120.84 32.61 120.96 82.01 60.86 32.50 237.78 240.66 196.17 128.70 202.05 190.26 146.70 194.74 32.38 7.91 132.87 109.44 21.06 55.30 191.75 44.61 31.95 35.20 64.80 14.00 28.77 3.83 14.01 104.32 55.19 105.97 63.94 86.26 85.56 109.84 140.90 63.55 45.59 143.72 34.76 118.28 100.18 17.78 25.72 32.67 27.54 32.06 170.29 118.93 17.88 13.50 27.14 24.28 34.68 30.98 45.94

On) 5.25 8.09 7.05 7.48 1.41 5.02 10.07 9.72 7.61 7.22 6.20 8.83 7.25 6.70 3.17 11.99 5.44 2.08 1.82 6.78 6.26 2.59 6.57 14.28 5.90 1.62 7.69 1.70 7.94 4.13 7.02 6.24 2.03 0.61 7.07 10.36 10.65 4.42 6.50 6.85 10.21 6.49 7.32 0.93 4.95 6.57 6.35 8.41 2.31 1.93 B.69 7.07 0.56 1.47 13.35 4.00 4.81 5.60 10.20 8.06 12.34 4.66 7.62 6.95 6.25 7.86 5.23 2.67 1.20 8.48 1.78 6.70 14.22 6.83 9.56

3.34 5.21 10.99 6.00 7.62 5.70 9.41 6.55 12.46 9.27 7.55 6.76 7.45 3.76 4.43 5.29 7.51 1.82 1.05 6.32 1.71 1.09 1.80 0.65 0.67 1.21 2.58 1.83 2.78 5.64 7.28 5.57 5.31 6.49 5.47 11.59 2.84 9.46 12.67 1.84 7.10 1.43 5.52 6.25 5.17 3.46 5.89 6.03 8.91 7.63 5.04 5.78 7.84 9.05 5.37 5.68 3.46

(ml 14.29 13.29 88.77 139.48 107.34 28.97 102.00 60.49 ' 101.75 17.46 134.88 10.78 1.01 20.05 7.04 1.15 -1.42 19.11 17.37 -19.10 -25.36 -21.25 20.82 -10.38 -17.65 10.55 14.94 6.97 B9.22 -15.57 14.66 25.56 -14.24 7.63 68.03 39.26 33.48 14.62 84.55 62.74 47.80 3.72 56.70 57.58 38.32 -40.36 -118.6 -131.5 -91.75 -162.7 -58.24 -99.22 -64.38 -43.62 5.70 -13.16 -17.09 -6.44 -3.18 10.74 11.05 5.72 -7.52 12.93 64.13 53.83 39.77 39.25 34.82 -17.24 15.56 2.12 -48.43 96.38 -62.67 -47.07 -26.77 93.26 -11.19 25.04 8.16 -3.97 9.16 39.32 67.13 -44.37 -38.73 -71.53 -44.60 -21.90 -31.06 20.19 6.21 104.03 145.86 18.28 68.60 127.33 107.95 -131.0 42.89 43.71 15.69 55.50 153.48 147.22 195.30 145.02 25.81 95.17 88.86 103.79 67.50 75.43 65.29 -53.19 46.68 34.45 -18.15 140.61 -65.47 53.01 122.67 103.75 83.20 78.90 62.28 -9.65 -4.22 133.27 128.39 119.62 112.33 48.95 65.28 122.11

(ml 9.04 5.20 B1.72 132.00 105.93 23.95 91.93 50.41 94.14 10.24 128.68 1.95 -6.24 13.35 3.87 -11.28 -7.10 17.03 15.55 -25.88 -31.62 -26.84 14.25 -24.66 -23.55 5.93 37.25 2.94 80.28 -19.70 7.64 19.32 -16.27 7.02 60.96 28.90 22.83 39.03 78.05 55.89 37.59 -2.77 49.38 56.65 33.37 -46.93 -125.40 -139.92 -94.06 -164.65 -66.93 -106.29 -64.94 -45.09 -13.42 -17.16 -21.90 -12.04 -13.38 2.68 -5.01 1.06 -15.14 5.98 57.88 45.01 34.04 36.26 33.62 -25.72 13.78 -4.28 -62.65 79.55 -72.23 -49.17 -31.75 86.55 -12.60 21.70 2.95 -14.96 3.16 31.70 61.43 -53.78 -45.28 -83.99 -53.87 -29.45 -37.82 12.74 2.45 99.60 140.57 10.77 62.26 123.28 101.63 -132.74 41.80 38.91 15.04 54.83 149.27 144.61 193.47 142.24 20.17 B8.19 83.29 98.48 61.01 69.96 51.67 -56.03 37.22 21.78 -22.99 133.51 -66.90 47.49 116.42 98.58 79.74 73.01 56. 25 -18.56 -11.85 128.23 122.61 111.78 103.28 43.58 59.60 118.37

DDH

R2691 R2692 R2700 R2709 R2710 R2714 R2715 R2716 R2729 R2763 R2764 R2766 R2767 R2768 R2769 R2770 R2771 R2772 R2773 R2774 R2775 R2776 R2777 R2778 R2779 R2780 R2781 R2782 R2783 R2784 R2785 R2786 R2787 R2788 R2789 R2790 R2791 R2792 R2793 R2794 R2795 R2796 R2797 R2798 R2800 R2801 R2802 R2803 R2804 R2805 R2806 R2807 R2809 R2813 R2814 R2815 R2S16 R2817 R2818 R2819 R2821 R2822 R2825 R2826 R2835 R2836 R2838 R2839 R2840 R2841 R2842 R2843 R2844 R2845 R2846 R2847 R2849 R2851 R2852 R2853 R2854 R2855 R2856 R2857 R2S58 R2859 R2860 R2861 R2862 R2863 R2864 R2870 R2872 R2873 R2874 R2875 R2876 R2877 R2878 R2879 R2894 R2898 R2899 R2900 R2901 R2902 R2903 R290S R2906 R2909 R2910 R2911 R2912 R2914 R2935 R2936 R2939 R2941 R2987 R2988 R2989 R2990 R2991 R2992 R2993 R2997 R2998 R3011 R3012 R3014 R3023 R3024 R302S R3026 R3028 R3033

EASTING (ml

98696.84 98456.92 97222.95 98714.93 98525.70 96513.67 96516.01 96491.06 97433.59 95300.76 96194.49 96254.12 96025.48 96739.02 96671.54 96399.18 96173.91 96444.79 96697.39 96951.71 96825.64 96806.74 96629.49 9624S.17 96317.25 96572.90 96122.98 96355.14 96490.05 96599.20 96160.16 96444.34 96707.17 96237.29 96083.76 96179.68 96487.78 96223.55 96614.63 96664.99 96895.91 96834.88 96463.14 96347.63 96424.13 96602.67 96853.81 96365.69 96412.47 96372.76 96149.85 96622.05 96888.79 98886.20 98661.54 98726.06 98608.23 98372.53 98655.90 98754.77 98393.91 99028.56 98432.27 98440.86 98111.87 97869.14 98339.17 98128.62 97869.60 97960.74 97893.53 98020.42 98139.57 97740.93 97667.62 97522.81 97910.76 97444.78 97390.82 97181.72 97159.64 97323.23 97421.56 97387.91 97549.67 97105.51 97714.48 97926.11 97986.57 97649.09 97615.08 98881.90 98532.82 98492.21 98417.18 98765.08 98836.30 98879.10 98920.65 98838.63 98967.39 97587.02 97714.49 97951.55 97603.46 98053.61 98178.00 97609.92 97866.76 97492.42 97993.96 98189.45 98227.92 97739.76 98719.97 98375.94 98669.45 98629.83 99045.02 98984.37 98949.43 98958.24 99047.71 99098.71 98994.35 98944.94 98952.27 98145.15 97587.35 97686.79 98037.78 97349.23 97477.67 97111.95 97085.82 97609.23

NORTHING (m)

195942.44 195945.19 195377.80 195501.55 195499.44 195248.48 195243.89 194598.45 194745.67 196339.14 195612.20 195876.44 195876.80 195864.11 195745.63 195753.73 195749.20 195627.69 195621.17 195614.38 195511.98 195619.56 195518.19 195495.25 195624.55 195623.94 195388.44 195378.45 195373.44 195370.02 195253.81 195245.78 195114.89 195124.88 195240.95 195126.61 195119.31 195360.89 195127.81 194993.08 194991.48 194874.23 194873.58 194876.61 194750.28 194881.47 195120.70 195122.98 195491.95 195874.06 195863.77 195870.45 195867.41 195128.80 195261.30 195368.73 195376.53 195387.02 195495.73 195502.20 195619.55 195643.50 195878.73 195512.95 194507.16 194507.80 194611.56 194621.44 194636.72 194741.98 194894.69 194866.59 194903.09 194777.52 194875.48 194871.31 195116.48 195000.44 194881.13 195129.31 195249.78 195131.44 195118.83 195227.28 195128.91 195130.91 195249.81 195244.83 195124.59 195193.41 195130.94 19S244.06 195768.22 195746.13 195749.55 195750.47 195748.52 195751.44 195503.22 195564.70 195567.84 194372.45 194378.31 194374.84 194610.56 194379.27 194376.09 194248.31 194264.77 194628.31 194626.12 194739.69 194621.59 194628.75 195870.80 195888.69 195926.69 195869.55 195395.17 195400.77 195412.20 195458.34 195451.92 19S449.52 195501.41 195320.11 195350.91 194374.63 194249.33 194259.02 195120.38 195371.64 195379.11 195376.83 195626.77 195372.53

COLLAR (ml

109.19 83.47 82.44 128.02 94.65 114.86 115.14 130.41 57.13 62.99 104.48 123.41 83.58 90.52 94.79 134.09 95.71 121.37 98.80 59.05 76.23 88.80 111.31 138.57 134.66 104.94 139.42 117.74 110.91 96.76 142.58 110.92 S5.66 147.21 151.83 153.21 131.48 134.17 101.71 117.81 93.90 106.13 143.88 147.35 128.56 139.71 86.51 135.24 144.29 118.79 36.43 93.34 68.34 98.97 99.50 113.39 104.11 84.79 122.41 130.86 69.62 178.28 78.38 90.30 117.72 129.22 72.47 109.64 162.94 127.33 117.39 103.12 62.47 127.05 108.99 78.61 92.13 102.64 62.12 49.44 18.71 99.60 113.68 92.82 134.90 37.12 133.27 68.15 71.18 154.46 145.98 112.48 81.81 B0.95 75.16 121.37 129.73 137.14 161.29 147.70 181.31 103.90 120.81 107.44 82.40 94.30 76.83 60.93 105.75 58.25 132.65 68.74 88.35 129.46 118.93 69.89 107.34 104.74 135.60 133.84 135.13 143.30 151.63 150.97 150.99 119.68 126.90 81.97 56.32 77.86 63.28 104.58 126.70 52.44 52.67 150.26

DEPTOP (ml

27.66 37.46 86.02 42.02 36.35 67.32 67.35 30.92 50.76 91.74 48.37 157.88 104.82 111.54 117.16 142.43 71.49 92.71 94.63 72.49 59.21 91.83 82.24 71.93 94.55 83.77 45.12 48.93 57.37 58.24 47.12 50.40 43.16 56.30 51.69 57.37 74.24 53.10 54.80 67.56 19.44 57.88 71.04 66.20 56.13 81.66 44.97 61.22 90.53 162.83 107.10 132.00 34.80 27.84 48.10 43.88 48.88 47.84 49.51 35.44 34.60 25.86 38.25 50.51 113.81 122.40 56.14 111.23 171.14 137.62 128.86 112.92 65.32 129.63 112.89 78.35 34.16 108.00 63.73 52.01 41.64 107.40 118.71 95.90 127.79 34.41 148.85 61.49 64.11 166.06 135.96 43.15 25.20 33.70 41.39 29.09 33.63 41.13 41.74 33.80 41.56 63.70 92.86 89.96 72.35 82.08 102.54 42.70 119.03 33.08 139.58 68.19 84.75 133.47 42.30 35.22 30.24 44.87 9.88 18.08 26.44 26.62 17.80 12.29 20.00 24.14 23.08 101.34 23.86 72.31 50.04 106.61 139.88 47.64 64.35 149.34

DEPBOT (ml 33.38 13.71 96.18 45.23 10.54 75.44 75.39 36.60 60.15 93.19 53.30 163.47 106.39 116.15 128.05 147.66 77.14 100.51 99.26 75.11 68.68 97.43 92.71 76.14 99.18 95.98 52.52 56.42 66.34 67.31 53.67 57.38 53.46 62.81 55.08 64.08 81.92 60.39 64.20 76.34 54.32 62.28 77.68 72.72 62.62 88.67 56.02 68.15 97.86 171.02 113.41 146.04 87.76 33.18 53.93 51.42 51.42 54.09 19.72 10.48 43.45 26.17 44.62 57.52 123.13 131.83 63.98 121.08 180.94 147.84 137.12 120.30 71.17 140.37 117.06 34.75 91.19 115.76 71.77 58.78 51.99 115.67 126.55 109.35 134.48 39.23 154.60 80.72 64.85 173.06 142.52 44.94 34.96 41.48 17.26 31.95 39.52 41.72 49.66 44.56 47.67 67.64 98.76 95.98 BO.43 38.99 110.16 56.44 125.04 41.55 150.26 75.65 92.33 142.38 15.11 13.24 37.12 16.87 16.00 26.09 32.94 34.42 23.46 16.41 27.14 32.91 32.44 109.10 35.68 33.67 54.58 109.07 148.16 56.28 65.74 157.02

THICX On I 5.72 6.25 9.69 3.21 3.39 B.12 3.04 7.68 9.39 1.45 4.93 5.59 1.57 4.61 10.89 5.23 5.65 7.80 4.63 2.62 9.47 5.60 10.47 4.21 4.63 11.89 7.40 7.49 8.97 9.07 6.55 6.98 10.30 6.51 3.39 6.71 7.68 7.28 9.40 B.78 1.88 1.40 6.64 6.52 6.49 7.01 11.05 6.93 7.33 11.19 6.31 12.98 2.96 5.34 5.83 6.78 2.54 6.25 0.21 5.04 3.16 0.31 6.37 7.01 9.32 8.91 7.84 9.85 9.43 10.22 8.26 7.38 5.85 10.74 1.17 6.40 7.03 7.76 8.04 6.77 10.35 8.27 7.84 11.15 6.69 4.03 2.75 3.69 0.74 7.00 5.40 1.79 3.26 7.78 5.87 2.86 5.89 0.59 7.92 10.76 6.11 3.94 5.90 6.02 B.08 6.91 7.62 13.74 6.01 8.47 10.68 7.46 7.58 8.91 3.11 8.02 7.18 2.00 6.12 3.01 6.50 7.80 5.66 1.12 7.14 3.77 9.36 7.76 11.82 11.36 3.75 2.46 B.28 8.64 1.39 7.68

TOPELEV

(ml 81.53 46.01 -3.58 86.00 58.30 17.54 47.79 99.49 6.37 -28.75 56.11 -34.47 -21.24 -21.02 -22.37 -8.34 24.22 28.66 1.17 -13.44 17.02 -3.03 29.07 66.64 40.11 21.17 94.30 68.81 53.54 38.52 95.46 60.52 42.50 90.91 100.14 95.84 57.24 81.07 46.91 50.25 14.46 48.25 72.84 81.15 72.43 58.05 41.54 74.02 53.76 -44.04 -20.67 -38.66 -16.46 71.13 51.40 69.51 55.23 36.95 72.90 95.42 35.02 152.42 40.13 39.79 3.91 6.82 16.33 -1.59 -8.20 -10.29 -11.47 -9.80 -2.85 -2.58 -3.90 0.26 7.97 -5.36 -1.61 -2.57 7.07 -7.80 -5.03 -3.08 7.11 2.71 -15.58 6.66 7.07 -11.60 10.02 69.33 56.61 47.25 33.77 92.28 96.10 96.01 119.55 113.90 139.75 40.20 27.95 17.48 10.05 12.22 -25.71 18.23 -13.28 25.17 -6.93 0.55 3.60 -4.01 76.63 34.67 77.10 59.87 125.72 115.76 108.69 116.68 133.83 138.68 130.99 95.54 103.82 -19.37 32.46 5.55 13.24 -2.03 -13.18 1.80 -11.68 0.92

BOTELEV [ml

75.81 39.76 -13.74 82.79 54.11 39.42 39.75 91.81 -3.02 -30.20 51.18 -40.06 -22.81 -25.63 -33.26 -13.57 18.57 20.86 -0.46 -16.06 7.55 -8.63 18.60 62.43 35.48 8.96 86.90 61.32 14.57 29.45 88.91 53.54 32.20 84.40 96.75 89.13 49.56 73.79 37.51 41.47 39.58 43.85 66.20 74.63 65.94 51.04 30.49 67.09 46.43 -55.23 -26.98 -52.70 -19.42 65.79 45.57 61.97 52.69 30.70 72.69 90.38 26.17 152.11 33.76 32.78 -5.41 -2.61 B.49 -11.44 -18.00 -20.51 -19.73 -17.18 -8.70 -13.32 -8.07 -6.14 0.94 -13.12 -9.65 -9.34 -3.28 -16.07 -12.87 -16.53 0.42 -2.11 -21.33 -12.57 6.33 -18.60 3.46 67.54 46.85 39.47 27.90 89.42 90.21 95.42 111.63 103.14 133.64 36.26 22.05 11.46 1.97 5.31 -33.33 4.49 -19.29 16.70 -17.61 -6.91 -3.98 -12.92 73.52 26.65 69.92 57.87 119.60 107.75 102.19 108.88 128.17 134.56 123.85 86.77 94.46 -27.13 20.64 -5.81 B.70 -4.49 -21.46 -3.84 -13.07 -6.76

Appendix 6.5 (confd)

DDH

R3034 R3035 R3036 R3057

EASTING (m)

97294.71 97715.28 97846.22 96950.58

R3059 R3235 R3257 R3262 R3281 R3282 R3284 R3301 R3304 R3305 R3306 R3308 R3309 R3310 R3311 R3312 R3313 R3311 R3315 R3316 R3317 R3318 R3319 R3320 R3321 R3322 R3323 R3326 R3328 R3329 R3331 R3333 R3334 R3335 R3336 R3352 R3362 R3363 R3365 R3366 R3367 R3387 R3398 R3402 R3408 R3448 R34S5 R3456 R3457 R3458 R3459 R3467 R3478 R3479 R3483 R3485 R34S7 R3488 R3489 R3490 R3494 R3503 R3504 R3505 R3506 R3508 R3509 R3510 R3513 R3513 R3516 R3526 R3530 R3531 R3533 R3535 R3537 R3570 R3571 R3S72 R3574 R3630 R3633 R363S R3639 R3694 R369S R3696 R3698 R3703 R3705 R3721 R3722 R3721 R3725 R3729 S3730 R3731 R3732 R3733 R3735 R3736 R3737 R3740 R3741 R3743 R3744 R3745 R3746 R3747 R3748 R3749 R3750 R3752 R3754 R3757 R3761 S3762 R3763 R3767 R3768 R3769 R3770 R3771 R3772 R3775 R3776 R3777 R3781 R3783 R3784 R3785

95572.32 98826.08 95347.41 92911.18 97994.46 98274.57 97722.12 99244.74 99266.77 99245.83 99015.96 99058.80 99404.13 99129.45 99052.43 98707.70 98647.49 98260.12 98383.50 98929.00 99038.61 98791.48 98609.39 98884.91 98682.08 98679.26 99601.42 99612.71 99585.28 99823.94 99259.97 99510.82 99904.96 99851.57 100010.11 97633.80 99184.90 99211.92 99506.73 99369.61 99914.60 97520.07 98643.58 99013.02 99005.59 98523.43 99076.51 98822.44 98755.06 98643.44 98733.67 98017.31 96470.81 96414.55 96634.97 96240.32 96169.26 96180.05 96243.89 96151.09 96923.07 98834.41 98824.30 98614.21 98942.27 98385.48 98899.35 98918.96 98862.85 98825.32 98784.60 97834.51 97721.75 97723.96 97656.00 97532.33 98344.20 98950.42 99066.85 99035.77 99087.69 97751.16 97913.25 98291.66 98248.27 96961.65 96391.69 96716.89 96093.44 96258.98 96812.00 98893.62 98875.27 98843.17 98830.57 98746.15 98821.88 98835.85 98868.28 98858.42 98840.36 98811.10 98721.22 98692.85 98647.10 98727.33 98714.39 98691.66 98643.18 98729.12 98696.13 98696.19 98650.67 98684.56 98782.75 98834.49 98735.63 98679.70 98647.61 98615.17 96607.44 98753.36 98776.02 98853.58 98790.48 98781.16 98736.00 98684.27 98939.30 98859.31 98821.94 98919.87

NORTHING (ml

195515.56 195375.56 195369.64 195778.08 196126.75 195300.31 195999.48 198495.44 196620.06 196820.86 197253.66 201382.25 201480.91 201740.23 201494.64 202250.91 201009.15 201020.73 200251.31 200246.27 200009.73 200231.42 200006.88 200542.53 200744.02 200757.08 200722.81 201011.02 201248.53 2014 63.61 203994.81 203748.05 203488.47 203490.41 203021.28 202983.33 203983.61 204245.22 204476.02 194772.59 202489.36 202249.69 203240.77 202745.73 203760.09 195087.52 200251.98 195753.31 195769.66 200567.94 195559.39 195426.72 195560.25 195431.56 195311.06 194868.70 194564.19 194586.00 194759.70 194824.23 195077.30 194972.73 194903.19 195128.91 195039.91 195S99.63 195253.92 195080.63 195102.14 195649.16 195611.64 195601.81 195599.30 195588.88 195577.81 194381.94 194302.69 194356.98 194329.25 194542.08 194441.19 198358.20 198396.03 198622.38 198841.63 194904.05 194628.63 194476.41 194509.53 195172.86 195338.72 195241.09 195441.14 195627.78 195491.98 195314.73 195308.50 195330.84 195316.77 195199.27 195228.81 195212.16 195139.17 195133.19 195202.50 195154.19 195529.14 195470.28 195450.59 195432.58 195445.70 195491.97 195486.19 195402.31 195378.45 195406.70 195331.91 195104.44 195542.95 195247.55 195514.23 195448.20 195411.02 195426.84 195448.64 195543.23 195214.48 195221.02 195189.80 195161.09 195227.88 195194.70 195613.63 195012.41 195070.92 195049.89

COLLAR

(«) 86.06 134.39 109.39 74.15 96.70 119.68 92.56 57.68 148.36 136.88 106.46 160.74 177.52 166.28 128.28 80.67 196.93 152.23 189.71 152.69 99.56 83.20 94.53 168.30 155.21 188.67 140.53 153.33 147.64 112.50 159.80 175.64 139.87 199.16 111.63 137.73 152.65 134.57 85.82 97.73 80.39 107.27 141.67 77.27 208.95 122.05 137.40 159.55 156.44 121.83 175.14 129.55 136.66 112.60 109.84 102.29 136.15 144.16 103.91 111.32 144.53 126.36 113.48 152.40 B4.60 146.61 111.64 60.00 91.18 69.60 164.47 164.73 159.00 144.84 138.22 121.75 106.12 116.87 93.70 78.17 86.70 177.10 173.64 173.80 158.72 132.85 172.89 107.34 114.86 61.06 107.83 76.14 130.53 127.05 78.43 105.31 105.06 110.66 110.93 101.29 106.03 102.59 99.82 99.28 102.20 99.49 129.88 121.83 116.69 119.23 120.06 123.26 119.82 117.76 111.74 113.86 105.07 69.89 131.32 109.24 129.55 119.47 113.01 109.87 109.48 130.68 105.38 106.90 98.26 92.92 108.57 96.89 147.33 83.48 B8.15 88.33

DEPTOP (ml

98,30 128.04 95.52 101.68 98.86 47,46 39,10 32.50 145.39 115.28 158.05 38,96 60,06 60.31 84.40 34.75 39.84 59.46 83.88 103.87 60.06 136.82 109.48 92.10 62.36 144.60 129.59 106.06 151.06 132.72 152.48 150.86 112.20 109.90 135.00 98.43 64.25 75.10 28.72 99.80 92.12 27.30 122.84 54.46 114.00 115.94 104.88 33.91 26.76 133.99 23.64 40.74 35.34 53.14 46.56 113.02 15.25 28.28 42.62 19.53 46.78 28.67 21.05 53.87 42.61 47.00 45.95 19.60 25.44 46.20 36.36 34.92 36.09 40.22 34.90 104.57 37.07 90.32 58.33 38.27 84.48 57.58 35.27 54.52 34.81 140.10 177.45 95.45 101.42 29.04 39.46 39.22 37.94 30.62 58.18 19.59 25.00 32.21 37.48 60.10 40.90 32.98 28.13 27.45 29.27 29.18 40.96 44.59 52.65 40.16 10.67 48.50 49.32 43.80 45.10 13.04 50.16 33.23 24.17 42.00 34.89 47.06 52.09 50.26 44.99 28.55 58.60 35.82 26.50 23.23 53.35 52.87 21.51 33.44 27.55 27.90

DEPBOT IB) 105.53 134.02 100.96 106.21 99.40 55.49 41.33 35.20 152.59 122.07 165.04 15.10 66.51 69.56 90.94 12.69 15.91 65.62 B7.18 108.86 68.42 142.77 120.90 98.37 67.76 150.58 133.39 111.92 156.55 138.92 157.79 156.07 119.25 115.80 140.92 104.52 68.83 81.31 32.26 109.95 98.53 36.28 129.26 60.67

120.00 122.00 110.99 35.26 31.03 141.25 27.64 18.68 38.08 54.54 52.28 120.44 21.20 33.62 19.61 25.42 52.33 33.53 27.38 60.28 54.83 17.60 53.56 21.50 31.20 16.70 15.33 39.14 17.92 53.93 13.12 110.IS 92.72 95.89 63.75 15.35 90.52 61.67 11.19 61.63 11.09 147.10 186.45 101.28 108.58 32.22 46.59 51.60 13.12 B5.25 68.58 28.63 27.00 38.00 13.71 60.60 50.92 11.21 33.65 33.23 38.00 30.37 41.83 49.90 54.40 46.47 17.00 49.00 49.65 50.10 50.85 19.00 53.90 33.66 32.17 18.70 39.90 49.18 54.59 51.61 46.52 38.00 60.08 44.71 29.25 24.43 61.92 60.03 26.59 39.05 33.70 34.12

THICK (is) 6.04 5.98 5.44 4.53 0.54 8.03 2.23 2.70 7.20 6.79 6.99 6.11 6.45 9.2S 6.51 7.94 6.10 6.16 3.30 4.99 8.36 5.95 11.42 S.27 5.40 5.98 3.80 5.86 1.34 6.20 5.31 5.21 6.35 5.90 5.92 6.09 4.58 6.21 3.54 10.15 6.41 3.98 6.12 .21 .00

6. 6. 6.06 6.11 1.32 1.27 7.26 1.00 7.94 2.74 1.40 5.72 7.42 5.9S 5.34 6.99 5.89 5.55 1.86 6.33 6.11 10.01 0.60 7.61 1.90 5.76 0.50 7.10 1.52 11.16 13.71 8.22 5.58 5.65 5.57

TOPELEV BOTELEV (J»>

-19.17 0.37 8.43 -32.06 -2.70 64.19 51.23 22.48 -4.23 14.81 -58.58 115.64 111.01 96.72 37.34 37.99 150.99 86.61 102.53 43.83 31.14 -59.57 -26.37 69.93 B7.45 38.09 7.14 41.41 -8.91 -26.12 2.01 19.57 20.62 83.36 -29.29 33.21 83.82 53.26 53.56 -12.22 -18.14 70.99 12.41 16.60 88.95 0.05 26.41 124.29 125.41 -19.42 147.50 30.87 98.58 58.06 57.56 -18.15 114.95 110.54 54.30 85.90 92.20 92.83 36.10 92.12 29.77 99.01 58.08 38.50 59.98 22.90 119.14 125.29 111.08 90.91 95.10 11.60 13.40 20.98 29.95 32.82

5 6.53 9.00 5.83 7.16 3.18 7.13 12.38 5.18 1.63 9.50 9.04 2.00 5.79 5.82 0.50 10.02 8.23 5.52 5.78 B.73 1.19 0.87 5.31 1.75 6.31 6.33 0.50 0.33 6.30 5.75 5.96 3.74 0.43 B.00 6.70 5.01 2.12 2.50 1.35 1.53 9.45 1.48 8.89 2.75 1.20 8.57 7.16 5.05 5.61 6.15 6.22

(ml -12.24 6.35 13.87 -27.53 -2.16 72.22 53.46 25.18 2.97 21.60 -51.59 121.78 117.46 105.97 43.88 45.92 157.09 92.77 105.83 18.82 39.50 -53.62 -11.95 75.20 92.85 14.07 10.94 47.27 -3.42 -20.22 7.32 24.78 27.67 39.26 -23.37 39.30 38.40 59.47 57.10 -2.07 -11.73 79.97 18.83 22.81 94.95 6.11 32.52 125.61 129.68 -12.16 151.50 B8.81 101.32 59.46 63.28 -10.73 120.90 115.88 61.29 91.79 97.75 97.69 92.43 98.53 41.99 99.61 65.69 40.40 65.74 23.40 128.11 129.81 122.91 104.62 103.32 17.18 19.05 26.55 35.37 39.90 2.22 119.52 138.37 119.28 123.91 -7.25 -4.56 11.89 13.44 32.02 68.37 36.92 92.59 16.43 20.25 85.72 80.06 78.45 73.45 41.19 65.13 69.61 71.69 71.83 72.93 70.31 88.92 77.24 64.04 79.07 79.39 74.76 70.50 73.96 66.61 70.82 54.91 36.66 107.15 67.24 94.66 72.41 60.92 59.61 64.49 102.13 16.78 71.08 71.76 69.69 55.22 11.02 125.79 50 .V01 60.60 60.43

-3.82 115.43 132.45 112.17 117.63 -14.25 -13.56 6.06 6.28 28.84 61.24 24.54 B7.41 41.80 9.85 76.68 78.06 72.66 67.22 40.69 55.11 61.38 66.17 66.05 64.20 69.12 38.05 71.93 62.29 72.76 73.06 74.26 70.17 67.66 60.89 64.86 51.17 36.23 99.15 60.54 B9.65 70.29 58.42 58.26 62.96 92.68 45.30 62.19 69.01 68.49 46.65 36.86 120.74 44.43 54.45 54.21

DDH

R3786 R3787 R3788 R3789 R3791 R3792 R3794 R.3795 R3796 R3797 R3798 R3800 R3801 R3803 R3804 R3805 R3806 R3808 R3809 R3810 R3811 R3814 R3815 R3816 R3817 R3818 K3819 R3820 R3821 R3822 R3824 R3825 R3828 R3832 R3844 R3857 R3859 R3860 P.3866 R3378 R3879 R3880 R3881 R3886 R3888 R3889 R3892 R3893 R3896 R3913 R3918 R3919 R3920 R3921 R3923 R3925 R3937 R3938 R3939 R3940 R3943 R3944 R3945 R3946 R3947 R3948 R3949 S3950 R3951 R3952 R3953 R3954 R3955 R3956 R3957 R3958 R3959 R3960 R3961 R3962 R3963 R3964 R3965 R3966 R3967 R3969 R3971 R3972 R3973 R3974 R3975 R3977 R3981 R3983 R3984 R398S R3986 R39S8 R3989 R3991 R3992 R3993 R3994 R3995 R3996 R3997 R3998 R4001 R4002 R4003 R4001 R4005 R4006 R4009 R4010 R4011 R4012 R4013 R4014 R4015 R4016 R4017 R4018 R4019 R4021 R4023 R4021 R1026 R402S R4029 R4030 R4031 R4033 R4034 R4035 R4036

EASTING (ml

98925.32 98566.46 98575.64 98561.47 98709.16 98677.43 98616.63 99016.93 98964.35 99022.68 98603.19 99021.75 99044.82 98985.38 98952.63 98957.12 98971.18 99006.63 99061.13 99040.98 99066.39 98544.97 98439.38 99092.51 99120.27 99141.86 98988.46 98527.97 98466.52 98416.63 98238.28 98223.25 98342.93 98340.83 98466.26 98559.32 98736.25 98773.26 98677.35 98702.05 98700.31 98682.44 98564.68 98612.46 99118.85 99080.06 99042.16 99031.69 98951.08 98659.60 99016.14 99038.55 99055.41 99001.74 99016.29 99122.73 99052.80 99039.80 98916.48 98908.17 98704.32 98753.83 98863.74 98861.82 98862.92 99006.07 98958.68 98804.76 98881.54 98625.17 98758.93 98664.26 98508.08 98619.41 98704.70 98836.03 98744.31 98665.81 98941.97 98498.41 98500.46 98383.80 98349.80 98536.01 98583.86 99089.62 99097.84 99082.09 99051.46 98995.28 98956.72 99024.80 99069.81 99142.49 99212.63 99226.51 99232.72 99147.03 99193.66 99164.54 99144.35 99066.90 99162.88 99171.49 99172.78 99167.99 99132.18 99190.52 99242.73 99221.81 99241.05 99262.86 99289.16 99199.11 99237.18 99184.22 99225.01 99140.55 99271.77 99244.58 99192.47 99190.19 99141.67 99108.76 99056.73 99207.28 99253.18 99243.49 99029.83 99061.32 99249.53 99212.17 99122.81 99150.23 99279.44 99286.61

NORTHING (ml

194978.28 195529.70 195563.41 195483.70 195130.08 195124.88 195126.03 195630.49 194995.09 195640.20 195205.13 194999.23 194991.33 195036.22 195000.38 195067.80 195102.91 195039.56 195021.38 195049.02 195038.16 195317.86 195245.41 195033.45 195032.06 195033.97 195070.91 195413.77 195452.05 195443.84 195502.84 195452.33 195562.55 195380.91 195120.56 195127.84 195119.58 194957.44 195171.09 195067.02 195025.70 195031.47 195263.36 195330.17 195025.48 195018.19 195083.41 195090.75 195049.73 195180.52 198392.88 198398.02 198442.02 198282.05 198353.59 198495.06 198314.44 198500.66 198674.89 198497.16 198500.61 198661.20 198796.53 198857.94 198916.23 198954.27 199008.41 198714.02 198185.20 198166.30 198169.84 198244.94 198006.95 198008.66 198076.13 198065.95 197999.88 197927.16 198065.17 198068.67 198161.94 198191.30 198264.06 198345.81 198501.86 198626.30 198410.66 198384.42 198357.16 198313.41 198283.34 198316.09 198552.25 198674.80 198692.77 198720.77 198815.11 198806.16 198805.53 198884.52 198933.56 198938.02 198550.77 198620.34 198591.58 198523.91 198468.31 198659.81 198695.44 198769.14 198788.61 198814.94 198787.08 198884.64 198875.63 198933.23 198932.75 198528.38 198849.27 198836.23 198589.86 198608.06 198486.19 198419.27 198336.86 198731.30 198872.75 198768.34 198744.92 198789.97 198923.86 198679.05 198447.11 198473.22 198866.23 198903.27

COLLAR (ml

71.62 93.04 93.52 98.57 76.37 71.03 62.46 163.54 77.45 163.20 88.20 75.02 73.53 81.27 77.32 B6.66 89.65 82.76 84.38 35.73 84.72 36.32 79.39 84.14 83.62 82.44 36.25 85.97 91.45 96.85 52.99 50.98 63.18 75.29 57.24 55.37 75.76 59.66 88.37 63.30 52.40 52.17 92.54 100.01 83.62 34.03 89.57 89.49 33.44 89.39 179.03 178.03 185.52 143.94 165.77 189.91 144.96 194.92 153.58 172.03 157.04 135.77 132.81 133.19 129.12 130.29 124.03 136.13 160.09 148.51 149.92 165.61 104.55 122.21 139.04 157.09 140.07 127.42 175.05 117.94 134.68 121.00 129.42 155.52 142.06 183.00 168.17 169.10 159.16 157.34 152.16 151.58 136.32 181.53 185.84 185.09 188.48 165.79 177.05 172.26 167.34 150.73 197.71 196.65 199.56 192.55 180.63 186.10 191.06 178.30 187.30 188.24 194.75 175.59 173.06 160.84 153.01 197.31 172.87 186.22 200.86 200.96 186.78 170.35 151.88 178.35 167.88 183.76 167.66 161.73 119.06 187.41 176.74 180.61 165.10 153.92

DEPTOP fm)

24.70 25.20 26.60 34.45 29.04 36.60 38.75 17.81 27.13 12.28 15.55 22.01 35.64 21.34 24.15 22.73 22.00 21.25 27.54 20.72 24.04 42.92 38.02 23.30 31.25 31.52 22.20 36.92 45.85 54.20 32.55 35.70 30.20 39.50 28.94 23.60 11.20 22.95 59.80 5.00 55.40 5.60 48.40 48.70 41.10 36.75 22.50 21.00 22.20 47.56 49.98 16.29 51.15 8.22 33.80 51.10 1.50 61.30 51.60 68.22 95.70 61.80 58.18 66.18 53.13 32.50 23.20 58.85 51.75 100.35 73.05 107.80 66.05 65.00 68.65 60.65 57.35 53.70 57.00 87.72 110.70 115.80 133.00 128.35 103.15 53.80 26.50 25.90 19.20 26.60 28.10 11.90 59.57 11.40 37.75 35.80 41.80 30.40 34.50 43.87 46.45 43.40 53.50 52.08 53.85 49.00 38.00 37.70 42.00 30.65 37.90 39.25 43.00 43.60 30.90 32.20 15.90 56.55 23.20 40.35 56.2S 54.00 43.40 27.50 8.00 31.80 22.90 36.10 50.45 40.95 6.00 39.00 33.98 41.00 15.55 6.00

DEPBOT (ml 30.25 26.91 31.20 37.24 31.78 37.05 39.27 19.19 34.42 13.00 52.22 30.58 36.64 27.90 31.52 29.90 26.00 28.41 37.06 29.78 32.42 47.28 46.34 33.46 36.23 37.15 30.50 39.60 51.70 60.95 39.65 11.28 36.80 11.90 35.65 31.65 15.15 29.80 60.60 6.77 55.80 7.00 53.28 52.00 12.15 10.78 29.50 21.00 29.50 54.78 56.17 51.85 50.94 10.95 37.57 58.42 3.00 67.95 57.35 73.20 93.90 66.82 64.15 72.62 60.60 36.00 28.50 63.35 60.10 107.25 81.45 115.30 73.40 72.65 75.75 67.20 65.35 60.15 64.35 95.42 117.75 122.40 140.00 135.55 109.75 61.60 32.40 32.15 23.25 29.50 31.50 17.25 66.40 51.60 45.05 41.37 49.45 37.03 41.15 50.34 52.28 50.20 61.08 59.37 61.30 54.25 45.30 44.75 12.50 38.85 15.15 44.30 43.50 19.62 36.75 38.25 22.10 63.30 29.55 17.05 59.35 59.80 50.90 39.20 10.70 38.90 28.95 40.30 57.50 47.50 12.25 11.60 41.35 42.00 20.85 9.08

THICK (ml 5.55 1.71 4.60 2.79 2.74 0.45 0.52 1.35 7.29 0.72 6.67 8.51 1.00 6.56 7.37 7.17 1.00 7.19 9.52 9.06 8.38 1.36 8.32 10.16 1.98 5.63 8.30 2.68 5.17 6.75 7.10 8.58 6.60 2.40 6.71 3.05 3.95 6.8S 0.80 1.77 0.40 1.40 1.88 3.30 1.35 1.03 7.00 3.00 7.30 7.22 6.19 5.57 6.79 2.73 3.77 7.32 1.50 6.65 5.75 1.98 3.20 5.02 5.97 6.14 7.17 3.50 5.30 1.50 5.35 6.90 8.40 7.50 7.35 7.65 7.10 6.55 8.00 6.45 7.35

70 05 60 00 20 30 80

5.90 6.25 4.05 2.90 3.40 2.35 6.83 7.20 7.30 6.07 7.65 6.63 6.65 6.17 5.83 6.80 7.58 7.29 7.45 5.25 7.30 7.05 0.50 .20 .55 .05 .50 .02 .85 .05

6.20 6.75 6.35 6.70 .10 80 50 35 70 10 05 20

7.05 6.55 6.25 5.60 7.37 1.00 5.30 3.08

TOPELEV (ml

46.92 67.84 66.92 64.12 47.33 34.43 23.71 145.70 50.32 150.92 42.65 52.98 37.89 59.93 53.17 63.93 67.65 61.51 56.84 65.01 60.68 43.10 11.37 60.81 52.37 50.92 64.05 49.05 45.60 32.65 20.44 15.28 32.98 35.79 28.30 31.77 64.56 36.71 23.57 58.30 -3.00 16.57 11.11 51.31 12.52 17.28 67.07 68.49 61.21 41.83 129.05 131.75 131.37 135.72 131.97 138.81 143.16 123.62 101.98 103.81 61.31 73.97 71.63 66.71 76.29 97.79 100.83 77.28 105.34 48.16 76.87 57.81 38.50 57.21 70.39 96.44 82.72 73.72 118.05 30.22 23.98 5.20 -3.58 27.17 38.61 129.20 141.67 143.20 139.96 130.71 124.06 136.68 126.75 137.13 118.09 149.29 146.68 135.39 142.55 128.39 120.89 107.33 144.21 144.57 145.71 143.55 142.63 148.40 149.06 147.65 149.40 148.99 151.75 131.99 142.16 128.64 137.11 140.76 149.67 145.87 144.61 146.96 143.38 142.85 143.88 146.55 144.98 147.66 117.21 120.78 113.06 148.41 142.76 139.61 149.55 147.92

BOTELEV Iml

41.37 66.13 62.32 61.33 14.59 33.98 23.19 144.35 43.03 150.20 35.98 44.44 36.89 53.37 45.80 56.76 63.65 54.32 47.32 55.95 52.30 39.04 33.05 50.68 47.39 45.29 55.75 16.37 39.75 25.90 13.31 6.70 26.38 33.39 21.59 23.72 60.61 29.86 27.77 56.53 -3.10 45.17 39.26 18.01 11.17 13.25 60.07 65.19 53.91 31.61 122.86 126.18 124.SB 132.99 128.20 131.49 141.96 116.97 96.23 98.83 58.14 68.95 68.66 60.57 68.82 94.29 95.53 72.78 99.99 41.26 68.47 50.31 31.15 49.56 63.29 89.89 74.72 67.27 110.70 22.52 16.93 -1.40 -10.58 19.97 32.31 121.40 135.77 136.95 135.91 127.84 120.66 134.33 119.92 129.93 140.79 143.22 139.03 128.76 135.90 121.92 115.06 100.53 136.63 137.28 138.26 138.30 135.33 141.35 148.56 139.45 141.85 143.91 151.25 125.97 136.31 122.59 130.91 134.01 113.32 139.17 141.51 111.16 135.88 131.15 141.18 139.45 138.93 143.46 110.16 114.23 136.83 142.81 135.39 138.61 144.25 144.84

Appendix 6.5 (cont'd)

DDH

R4037 R4040 R4041 R4045 R4046 R4048 R4050 R4052 R4053 R4054 R4055 R40S6 R4057 R4058 R4059 R4060 R4061 R4062 R4063 R4064 R4065 R4066 R4067 R4068 R4069 R4070 R4071 R4072 R4073 S4074 R4075 R4076 R4077 R4078 R4079 R4080 R4081 R4082 R4083 R40S4 R4085 R1086 R4087 R4088 R4089 R4090 R4091 R4134 R413S R4137 R4139 R4139 R4140 S4141 R4142 R4143 R4144 R4145 R4149 R4153 R4156 R4157 R43SS R4159 R4160 R4161 R4162 R4163 K4164 R4167 R4168 R4178 R4180 R4182 R4183 R4184 R4185 R4186 R4187 R4188 R1189 R4190 R4191 R4192 R4193 R4195 R4198 R4199 R4200 R4201 R4202 R4204 R4210 R4211 R4212 R4225 R4229 R4230 R4231 R4232 R4233 R4234 R4237 R4240 R4333 R4337 R4338 R4339 R4342 R4344 X4345 R4467 R4468 R4469 R4472 R4S32 R4534 R1535 R4538 R4541 R4542 R4543 R4545 R4546 R4547 R4548 R4549 R4S52 R4554 R4570 R4571 R4S74 R4622 R4623 R4624 R4627

EASTING (ml

99275.42 98911.84 99172.14 99098.53 99271.74 99272.63 97866.80 96248.05 96303.36 96436.11 96498.66 96159.68 96234.53 96371.91 96484.69 96463.93 96406.74 96475.81 96536.23 96599.93 96652.29 96681.99 96723.54 96776.10 96350.46 96838.35 96894.18 96942.62 96321.73 96297.25 96412.81 96275.94 96304.46 96334.73 96258.59 96410.47 96406.32 96538.49 96155.25 96300.51 96411.35 96575.31 96490.50 96537.26 96650.88 96622.10 96716.56 96381.53 96385.33 96309.77 96412.36 96445.71 96460.49 96493.06 96492.40 96533.46 96526.24 96555.31 96667.15 96935.45 96937.93 96957.02 96857.21 96809.65 96871.12 96873.08 96899.04 96896.49 96310.32 96623.83 96874.76 97808.51 97744.52 97643.12 97696.23 97631.55 97640.51 97560.79 97536.23 97563.81 97574.55 97550.91 97502.75 97466.65 97435.41 97944.94 98009.54 98132.91 98151.32 98014.35 98001.09 98017.12 97682.60 97755.14 97819.89 97609.90 97895.35 97827.87 97937.14 97880.58 97738.98 97595.68 97756.50 97617.06 97670.4 7 97810.00 97760.00 97781.39 96198.68 96564.48 96625.49 96589.04 96648.65 96701.07 96671.43 98996.37 98995.79 99009.72 98938.29 98838.60 98822.58 96794.38 98564.59 98526.72 98532.94 98543.01 98588.01 98632.61 98503.82 98965.88 98949.14 98661.69 98100.73 97999.57 97996.85 97900.30

NORTHING (ml

198932.39 198461.55 198563.78 198393.48 198794.81 198914.31 194210.73 195076.20 195068.69 195063.95 195059.97 195192.48 195195.66 194761.84 194741.69 194681.41 194813.23 194818.19 194806.88 194815.17

194802.91 194873.66 194823.45 194801.59 194825.56 194805.95 194795.80 194863.05 194693.98 194822.30 194871.44 194943.47 194896.38 194931.33 194998.55 194950.39 195002.06 194930.88 195296.20 195252.69 195300.19 195182.72 195181.27 195288.81 195297.83 195196.31 195291.84 194603.13 194570.63 194589.28 194601.84 194580.52 194605.34 194S49.02 194576.09 194597.81 194577.56 194593.80 194628.84 194552.73 195059.27 195034.88 195067.66 195167.98 195316.69 195139.98 195111.03 195076.08 194590.30 194628.06 194479.02 194458.23 194455.22 194495.06 194457.88 194447.56 194381.38 194375.16 194443.70 194151.63 194476.02 194503.19 194550.14 194594.06 194633.95 194454.30 194442.55 194428.98 194399.44 194364.30 194346.23 194329.81 194294.41 194322.44 194277.25 194183.98 194332.14 194352.89 194510.16 194581.89 194557.45 194421.33 194687.34 194672.55 194226.59 194245.00 194280.00 194406.31 194936.19 194681.63 194689.80 194612.20 194627.08 194631.13 194658.45 194871.77 194894.59 194903.77 194844.45 194833.80 194857.16 194873.09 195040.34 195084.09 195008.84 195027.83 194995.28 194951.81 195040.38 194847.22 194825.91 194968.34 194361.72 194295.69 194281.81 194282.77

COLLAR Im)

152.38 179.59 198.38 161.30 192.51 151.16 92.03 152.68 149.83 145.86 141.07 146.48 136.36 137.84 117.41 115.24 139.08 129.75 121.46 118.22 117.60 122.20 108.27 96.67 147.38 93.36 82.53 88.05 124.12 131.15 149.77 133.46 134.98 147.25 142.53 167.21 159.70 154.36 142.58 121.82 107.16 102.62 124.76 103.88 B8.52 92.27 73.56 139.61 140.87 117.35 143.14 135.65 128.11 130.48 130.74 115.48 115.78 106.49 81.61 73.28 78.19 78.29 94.98 98.20 53.84 32.03 79.99 82.29 117.48 93.19 100.22 129.04 135.76 114.21 137.63 116.60 116.31 106.61 92.43 94.23 92.81 B6.09 69.84 50.24 39.50 120.22 113.42 102.65 91.12 100.33 97.58 90.35 91.65 94.09 96.95 49.33 105.60 107.25 126.81 139.43 120.40 109.86 136.61 93.10 70.15 92.00 B7.50 126.80 116.87 101.86 95.28 101.12 85.00 74.50 B4.17 45.39 47.66 18.22 40.53 36.94 37.47 39.77 42.37 42.31 44.49 44.63 44.72 42.10 42.98 13.01 10.02 12.77 B8.66 B1.07 81.23 105.46

DEPTOP (ml

4.80 73.40 52.60 15.95 47.00 3.00 116.72 61.30 64.34 78.08 79.91 49.16 48.92 60.10 48.54 47.24 63.75 58.50 54.92 56.77 59.54 68.80 53.31 15.14 67.47 42.34 35.15 41.16 42.73 46.07 72.99 43.56 50.76 63.41 50.72 88.50 B2.67 91.22 18.31 13.06 41.28 57.06 71.76 58.27 49.04 51.89 35.46 33.13 20.42 4.70 37.26 20.27 28.48 11.OO 18.36 20.00 6.36 7.74 7.15 3.00 39.68 33.80 48.87 51.27 21.83 13.32 38.35 38.13 5.11 15.30 12.70 119.93 118.70 85.78 114.76 83.58 81.14 64.48 17.95 50.70 51.72 14.53 26.86 10.66 6.02 101.72 92.76 91.08 100.80 89.92 95.62 101.84 65.55 77.22 96.86 124.44 91.00 90.48 113.34 139.48 113.60 70.35 143.01 98.71 94.75 102.00 86.54 109.74 19.88 39.60 33.23 13.55 10.76 7.80 25.38 34.52 54.12 47.94 22.44 13.90 13.93 13.23 9.67 10.58 19.36 17.55 10.45 9.25 18.42 32.50 44.33 11.10 97.00 112.61 126.65 109.31

DEPBOT Im) 9.85 78.35 60.05 23 .10 17.20 8.10 119.08 67.91 70.97 35.38 37.03 55.70 55.27 66.50 55.17 53.93 69.88 65.00 61.57 63.73 67.00 76.20 61.41 54.00 73.80 48.30 38.30 42.94 48.99 52.46 79.52 50.35 57.06 70.39 56.84 94.89 89.50 98.57 55.22 49.49 18.22 66.46 79.66 70.80 61.87 61.41 47.12 40.33 22.40 6.26 44.32 27.80 35.75 12.74 26.32 28.06 33.91 15.51 14.48 1.30 13.50 10.86 59.28 61.22 36.10 51.86 19.67 17.15 6.76 24.60 13.10 132.38 125.67 93.44 123.58 91.88 B7.12 66.90 49.40 56.74 59.42 50.70 33.28 15.78 11.04 107.38 98.37 97.08 110.46 96.90 102.05 108.33 71.28 83.20 102.76 133.90 96.74 96.07 119.77 148.52 122.08 78.60 152.46 107.77 103.55 107.94 95.00 115.66 26.16 46.28 40.10 22.20 16.93 11.30 32.05 39.94 59.40 55.38 26.29 15.90 14.91 15.82 22.50 19.98 26.56 25.20 15.52 15.10 25.21 38.10 19.32 12.25 104.35 118.75 133.28 115.57

THICK Im) 5.05 4.95 7.45 6.82 0.20 5.10 2.36 6.61 6.63 7.30 7.12 6.51 6.35 6.10 6.63 6.69 6.13 6.50 6.65 6.96 7.16 7.10 8.13 3.86 6.33 5.96 3.15 1.78 6.26 6.39 6.53 6.79 6.30 6.95 6.12 6.39 6.83 7.35 6.91 6.43 6.91 9.10 7.90 12.53 12.83 9.52 11.66 7.20 1.98 1.56 7.06 7.53 7.27 1.71 7.96 8.06 7.58 7.80 7.33 1.30 1.97 6.11 10.41 9.95 11.57 11.54 11.32 8.72 1.62 9.30 0.40 9.50 6.97 7.66 8.82 8.30

98 90

9.46 5.74 5.59 6.43 9.01 8.18 8.25 9.12 9.03 S.80 5.94 B.46 5.92 6.28 6.68 6.87 8.65 6.17 3.50 6.67 5.42 5.28 7.41 3.81 2.00 1.01 2.59 7.51

6.82 5.60 1.99 1.15 7.35 6.11 6.63 6.23

TOPELEV (m)

117.58 106.19 145.78 145.35 145.51 149.16 -24.69 91.38 85.49 67.78 61.16 97.32 87.44 77.74 68.87 68.00 75.33 71.25 66.51 61.45 58.06 53.40 54.96 51.53 79.91 51.02 47.38 46.89 81.39 85.08 76.78 39.90 B4.22 83.83 91.81 78.71 77.03 63.11 94.27 78.76 65.88 45.56 53.00 45.61 39.48 40.38 38.10 106.48 120.45 112.65 105.88 115.38 99.63 119.48 112.38 95.48 109.42 98.75 74.46 70.28 38.51 44.49 46.01 36.93 29.01 38.71 11.61 13.86 112.31 77.89 37.52 9.11 17.06 28.13 22.87 33.02 35.17 12.13 11.48 43.53 41.09 11.56 12.99 39.58 33.18 18.50 20.66 11.57 -9.68 10.11 1.96 -11.49 26.10 16.87 0.09 -75.11 14.60 16.77 13.47 -0.05 6.80 39.51 -6.43 -5.64 -24.SO -10.00 0.96 17.06 96.99 62.26 62.05 87.57 74.24 66.70 58.79 10.87 -6.46 0.28 18.09 23.04 23.51 26.51 32.70 31.73 25.13 27.06 31.27 32.85 21.56 10.5 4 -1.31 31.67 -8.34 -28.57 -12.12 -3.88

BOTELEV

112.53 101.21 138.33 138.20 145.31 143.06 -27.05 84.74 78.86 60.48 54.04 90.78 81.09 71.34 62.21 61.31 69.20 61.75 59.89 54.49 50.60 46.00 46.83 42.67 73.58 45.06 41.23 15.11 75.13 78.69 70.25 B3.ll 77.92 76.86 35.69 72.32 70.20 55.79 87.36 72.33 58.91 36.16 15.10 33.08 26.65 30.86 26.14 99.28 118.17 111.09 93.82 107.85 92.36 117.71 104.42 87.42 101.84 90.95 67.13 68.98 34.69 37.43 35.60 26.98 17.44 27.17 30.32 35.14 110.72 68.59 87.12 -3.34 10.09 20.77 14.05 24.72 29.19 39.71 43.03 37.49 33.39 35.39 36.56 31.16 28.16 12.84 15.05 5.57 -19.34 3.43 -4.47 -17.98 20.37 10.89 -5.81 -84.57 8.86 11.18 7.04 -9.09 -1.68 31.26 -15.85 -14.67 -33.40 -15.94 -7.50 11.14 90.71 55.58 55.13 78.92 68.07 63.20 52.12 5.45 -11.74 -7.16 14.25 21.04 22.53 23.95 19.87 22.33 17.93 19.41 29.20 27.00 17.74 1.94 -9.30 30.52 -15.69 -34.68 -49.05 -10.11

DDH

R4630 R4631 R4634 R4635 R4636 R4637 R4638 R4639 R4640 R4641 R4642 R4644 R4645 R4646 R4647 R4648 R4650 R4651 R4652 R4653 R4654 R4655 R4656 K4657 R4658 R4660 R4661 R4669 R4676 R4677 R4678 R4683 R4684 R4685 R4686 R4687 R4690 R4691 R4692 R4693 R4694 R4695 R4696 R4698 334699 R4709 R4711

R4715 R4716 R4717 R1719 R4724 9.4 7 25 R4726 R4729 R4730 R4733 R4734 R4736 R4738 R4744 R4745 R4749 R4750 R4753 R4754 R4756 R4757 R4758 R4759 R4760 R4761 R4762 R4763 R4764 R4765 R4767 R4768 R4777 R4784 R4788 R4792 R4793 R4794 R4799 R4801 R4802 R4804 R4808 R4810 R4811 R4813 R4815 R4816 R4817 R4819 R.4821 R4822 R4823 R4827 R4829 R4831 R4834 R.4836 R4837 R4842 R4843 R4845 R4960 R5OO0 R5001 R5002 R5004 R5007 R500S R5009 R5010 R5011 R5012 R5013 R5011

R5015 R5016 R5017 R5018 R5019 R5020 R5022 R5024 R502S R5026 R5027 R5028 R5029 R5030 R5031

EASTING

(m) 97594.16 97529.24 97475.64 97637.80 97569.01 97490.60 97697.14 97344.69 96478.43 98411.51 98435.73 98381.31 98440.86 98474.48 98504.94 98S00.55 98322.82 98249.80 98309.28 98261.07 98402.69 98452.30 98413.31 98437.12 98393.03 98051.77 98048.79 98396.27 97579.63 97621.77 97605.16 97622.10 97600.77 97577.21 97523.61 97481.70 97453.84 97428.10 97568.24 97587.19 97635.92 97639.63 97649.91 97551.74 97548.40 98406.92 98571.52 98561.08 98420.71 98534.21 98541.13 98299.04 98314.73 98306.59 98193.34 98229.51 98217.20 98322.76 98317.20 98374.61 98183.05 98217.68 98343.98 98301.89 98840.91 98787.08 98789.60 98760.07 98777.98 98794.36 98685.00 93989.68 98927.95 98898.67 98863.01 98831.55 98503.78 98521.35 98418.78 98748.04 98409.32 98657.34 98734.22 98361.38 98513.41 98432.02 98569.31 98410.49 98512.03 98574.44 98366.72 98412.20 98253.11 98393.40 98388.47 98147.22 98163.40 98568.70 98600.07 98235.65 98294.46 98542.45 98590.59 98843.28 98938.30 98732.65 98702.50 98750.42 99209.39 97599.14 97604.13 97649.60 97699.22 97698.83 97519.79 97747.51 96748.92 96500.11 96450.95 96451.34 96500.14 96352.69 96402.20 96550.63 1 96549.85 1 96548.54 1 96596.94 96599.68 96691.67 3 96698.56 1 96160.39 3 96159.00 1 96203.12 1 96191.79 1 96160.14 I 96192.09 1

NORTHING (ml

194347.42 194523.89 194552.08 194854.73 194867.20 194867.23 194797.13 194894.88 194438.98 194442.41 194494.41 194555.19 194550.89 194587.83 194560.02 194592.72 194558.66 194679.34 194668.48 194754.56 194643.34 194632.02 194649.41 194660.48 194670.50 194346.98 194315.41 194390.49 194245.23 194265.42 194267.27 194359.30 194365.13 194422.92 194537.02 194569.44 194610.20 194616.19 194391.38 194399.69 194322.02 194288.11 194243.70 194232.41 194262.91 195574.09 195599.45 195673.05 195811.59 195811.08 195698.73 195558.91 195460.63 195440.81 195586.88 195675.78 195707.67 195314.88 195346.27 195437.05 195442.64 195563.84 195759.72 195804.69 195900.69 195935.13 195809.84 195907.49 195906.81 195878.25 195983.05 195819.98 195777.83 195777.09 195781.59 195811.91 195873.73 195916.56 194991.91 195803.20 195942.02 195901.23 195768.55 195885.70 195569.02 195694.03 195708.14 195650.34 195449.28 195428.34 195369.69 195366.30 195444.13 195365.11 195322.47 195510.06 195439.31 195448.39 195414.41 195594.36 195602.19 195542.69 195586.23 195740.98 195760.73 195840.94 195906.97 195800.45 198612.20 194232.41 194214.98 194208.09 194219.83 194238.63 194218.48 194254.80 194685.42 194596.38 194602.95 194622.00 194616.48 194622.61 194622.66 194596.48 194623.45 194643.05 194601.89 194646.33 194638.73 194669.61 195088.84 195377.13 195005.66 294985.59 195053.81 195038.63

COLLAR (ml

93.07 78.22 63.36 102.40 86.16 74.58 113.63 67.04 54.91 68.03 74.75 78.23 73.07 59.15 55.03 49.95 83.35 70.87 71.58 54.47 64.79 59.94 59.32 55.31 59.03 84.38 80.15 76.60 59.39 66.56 66.14 101.80 102.15 113.40 74.12 65.96 52.26 44.60 119.24 120.33 93.96 83.42 75.17 57.91 64.39 74.41 94.71 93.70 71.90 86.66 88.59 58.13 61.46 61.08 43.85 11.59 12.09 51.00 56.56 66.67 11.57 13.81 60.40 55.83 113.80 112.56 125.13 119.43 120.39 123.43 102.14 142.00 140.58 139.29 135.65 133.03 84.97 39.84 32.65 120.72 78.47 112.23 119.41 67.91 90.37 85.09 92.04 74.55 95.08 91.03 66.87 66.25 53.48 66.91 65.07 38.61 39.29 91.71 34.07 44.06 53.06 91.08 97.03 133.93 146.42 120.03 116.22 120.68 171.81 69.77 66.21 70.58 77.06 82.10 56.63 83.60 77.11 110.52 110.49 111.45 110.98 111.61 111.55 109.43 109.71 106.78 100.03 99.37 77.51 79.19 142.08 147.85 121.55 119.41 125.80 124.90

DEPTOP DEPBOT Iml

52.85 36.76 19.40 104.50 86.10 74.34 111.80 67.86 52.06 84.74 75.09 67.09 66.41 51.15 19.00 42.90 66.25 66.70 60.15 47.84 55.63 51.40 17.02 18.56 12.10 92.17 121.00 128.80 30.70 29.30 26.90 62.10 62.50 63.40 36.40 16.40 5.65 33.60 71.70 72.90 48.40 42.50 70.50 28.90 37.10 40.95 24.90 24.20 34.10 29.60 27.93 27.95 40.12 40.20 24.65 11.20 6.68 9.83 19.50 10.90 31.55 22.21 33.8S 16.25 16.85 26.10 36.10 32.22 31.95 33.05 24.25 12.82 24.65 29.85 35.30 37.40 33.34 10.00 9.95 32.02 37.00 13.80 31.48 35.60 35.50 51.16 30.03 12.11 13.35 33.15 27.35 24.47 34.87 23.70 20.25 27.16 30.70 31.40 26.28 18.45 17.90 29.70 23.80 43,20 29.50 19.00 33.05 32.10 24.90 65.70 92.95 114.70 113.85 36.98 81.76 86.28 26.58 11.05 10.45 22.74 23.36 16.11 18.90 11.70 30.08 40.18 5.30 33.96 12.90 26.30 15.35 58.00 24.06 22.05 27.82 26.92

(ml 54.50 42.64 21.00 110.23 91.63 80.86 122.79 76.63 56.34 93.14 31.83 72.85 73.36 57.86 55.89 47.29 72.72 73.35 68.10 54.91 62.71 58.46 56.16 56.18 53.55 98.62 128.93 138.10 39.80 37.65 28.95 67.55 66.46 71.58 11.72 21.65 14.15 36.30 80.95 81.40 53.60 47.95 79.60 40.10 48.50 15.55 31.65 31.20 40.40 37.60 32.15 30.65 47.15 49.60 27.90 16.90 15.30 11.33 22.98 47.95 39.00 26.98 39.15 16.85 13.85 27.20 42.05 36.90 35.90 36.45 26.30 17.32 30.45 35.90 40.80 42.56 39.48 18.00 11.25 34.52 43.10 46.30 35.29 41.15 44.80 57.16 33.34 48.10 45.50 35.45 30.45 32.86 44.55 30.90 25.55 34.50 38.28 33.16 28.44 21.70 19.85 34.70 31.07 43.80 35.62 50.25 40.65 42.55 27.80 77.00 99.10 122.00 121.30 94.10 94.80 92.70 33.20 18.54 17.64 30.26 30.92 23.72 26.20 20.05 37.94 18.40 12.35 11.60 20.16 32.30 50.00 65.42 30.28 27.70 31.05 32.00

THICK Im) 1.65 5.88 1.60 5.71 5.53 6.52 10.99 8.77 4.28 8.40 6.74 5.76 6.92 6.71 6.89 4.39 6.47 6.65 7.95 7.07 7.08 7.06 9.14 7.62 10.15 6.45 7.93 9.30 9.10 8.35 2.05 5.45 3.96 3.18 5.32 5.25 7.65 2.70 9.25 8.50 5.20 5.45 9.10 11.20 11.40 4.60 6.75 7.00 6.30 8.00 1.22 2.70 .03 .10 .25 .15 .37 .50

TOPELEV BOTELEV

7. 9. 3. 1 . 7. 1. 3.48 7.05 7.45 1.77 5.30 0.60 2.00 0.80 5.65 1.68 3.95 3.40 2.05 4.50 5.80 6.05 5.50 5.16 6.11 8.00 30

2.50 6.10 2.50 0.81 5.55 B.10 6.00 3.31 5.99 2.15 2.30 3.10 8.39 9.69 7.20 5.30 7.31 7.58 1.76 2.16 3.25 1.95 5.00 7.27 0.60 6.12 1.25 7.60 5.25 2.90 11.30 6.15 7.30 7.15 7.12 13.01 S.12 6.62 7.49 7.19 7.52 7.56 7.28 7.30 B.35 7.86 7.92 7.05 7.64 7.26 6.00 1.35 7.12 6.22 5.65 3.23 5.08

Iml 10.22 11.46 43.96 -2.10 0.06 0.24 1.83 -0.82 2.85 -16.71 -0.31 11.14 6.63 8.00 6.03 7.05 17.60 4.17 11.43 6.63 9.16 8.54 12.30 6.75 16.63 -7.79 -40.85 -52.20 28.69 37.26 39.24 39.70 39.65 50.00 37.72 49.56 46.61 11.00 47.54 47.43 45.56 10.92 1.67 29.01 27.29 33.46 69.83 69.50 37.80 57.06 60.66 30.18 21.34 20.88 19.20 33.39 35.41 11.17 37.06 25.77 10.02 21.63 26.55 39.58 96.95 36.16 B8.73 B7.21 88.44 90.38 77.89 129.18 115.93 109.44 100.35 95.63 51.63 49.84 22.70 88.70 41.47 68.43 84.93 32.31 54.87 33.93 62.01 32.44 51.73 57.88 39.52 41.78 18.61 43.21 44.82 11.45 8.59 60.31 57.79 25.61 35.16 61.38 73.23 90.73 116.92 71.03 83.17 88.58 146.91 4.07 -26.74 -44.12 -36.79 -4.88 -25.13 -2.63 50.53 99.47 100.04 88.71 87.62 95.17 92.65 97.73 79.63 66.30 94.73 65.41 64.61

53.19 96.73 89.85 97.49 97.36 97.98 97.98

Iml 38.57 35.58 42.36 -7.83 -5.47 -6.28 -9.36 -9.59 -3.43 -25.11 -7.08 5.38 -0.29 3.29 -0.86 2.66 11.13 -2.48 3.48 -0.44 2.08 1.48 3.16 -0.87 5.48 -14.24 -48.78 -61.50 19.59 28.91 37.19 34.25 35.69 41.82 32.40 44.31 38.11 8.30 38.29 38.93 40.36 35.47 -4.43 17.81 15.89 28.86 63.06 62.50 31.50 19.06 56.44 27.48 14.31 11.48 15.95 27.69 26.79 39.67 33.58 18.72 2.57 16.86 21.25 38.98 94.95 B5.36 B3.08 82.53 84.49 86.98 75.84 124.68 110.13 103.39 94.85 90.47 45.49 41.84 21.40 B6.20 35.37 65.93 94.12 26.76 45.57 27.93 58.70 26.45 49.58 55.58 36.42 33.39 3.93 36.01 39.52 4.11 1.01 58.55 55.63 22.36 33.21 56.38 65.96 90.13 110.80 69.78 75.57 78.13 144.01 -7.23 -32.89 -51.42 -44.24 -12.00 -38.17 -9.10 43.91 91.98 92.85 81.19 80.06 87.89 85.35 89.38 71.77 58.38 87.68 57.77 57.35 17.19 92.08 82.43 91.27 91.71 94.75 92.90

Appendix 6.5 (cont'd)

DDH

RS034 R5035 XS036 R5038 K5039 R5040 R5041 R5042 R5043 R5044 R5045 R5046 R5047 RS048 R5049 R5055 R5058 RS059 R5060 RS062 R5063 R5061 R5065 R5070 R5071 R5072 R5073 R5071 R5076 R5078 R5082 R5083 R5081 R5085 R5086 R5087 R5088 R50B9 R5093 R5091 R5095 R5097 R5099 R5100 R5101 R5102 R5105 R5106 RS113 R5311 R5115 R5116 R5117 R5118 R5119 R5120 R5121 R5122 R5124 R512S R5126 RS127 R5161 R5162 R5163 R5164 R5175 R5177 R5179 R5180 R5181 R5383 S5184 R5185 R5186 R5187 R5188 R5189 R5190 R5191 R5192 RSI 93 RSI 95 R5196 RS197 R5198 R5199 R5255 R5256 R5257 R5258 R5259 R5260 R5262 R5264 R5265 R5266 R5267 R5268 R5269 S5273 R5272 R5273 R5274 R5300 R5301 R5302 RS305 R5306 R5307 R5308 R5309 R5320 R5321 R5333 R5334 R5335 RS336 R5337 R5338 R5339 R5340 R5343 R534S R5346 R5347 R5348 R5349 R5350 R5353 R5352 RS353 R5354

R5355 RS3 57 R5358

EASTING Im)

96745.50 96796.59 96797.76 96450.27 96400.56 96347.33 96345.56 96400.63 96499.57 96499.00 96449.80 96842.26 96496.26 96590.21 96642.58 97093.71 96895.77 96953.60 97049.57 97162.11 97212.68 97207.87 97156.24 97208.16 97156.57 97177.15 97129.08 97104.36 97105.81 99185.55 99167.12 99151.45 96749.14 96833.04 96898.44 96938.10 97057.60 97051.80 969S7.91 96900.93 96134.01 96084.21 96121.27 96114.88 96116.26 96073.82 96140.24 96065.17 96725.98 96778.83 96810.79 96739.99 96772.88 96857.70 96886.74 96536.16 96927.05 96568.72 96986.34 96668.35 97016.51 96922.20 97045.79 96908.03 96936.77 97034.04 98349.54 98299.26 98397.72 96130.21 96140.51 96119.55 96117.21 96102.18 96111.36 96307.05 96296.72 96355.32 96354.73 96419.77 96444.75 96596.36 96221.02 96278.57 96319.58 96298.71 96474.87 98080.92 98118.40 98084.32 97986.98 97989.17 97969.29 97926.62 97976.54 98024.31 98043.96 98088.93 98061.82 98099.17 98115.22 98014.38 97998.58 98035.60 96672.94 96755.52 96778.74 96968.46 96971.92 96957.69 96983 .92 96412.48 96225.34 96321.35 99001.01 98026.26 98033.51 97990.64 97977.99 98003.13 97938.26 97959.42 97965 .08 98000 .45 98115.24 98115.67 97991.13 97932.22 97930.65 98081.76 98093.77 98033.84 97990.23 97979.67 97991.84 97928.16

NORTHING Im)

194659.31 194654.02 194690.27 194657.28 194654.25 194656.98 194675.31 194672.86 194678.70 194698.00 194673.56 194689.48 194631.73 194669.52 194675.94 194606.55 194691.19 194753.84 194709.80 194756.14 194754.61 194708.63 194710.23 194681.98 194684.91 194807.94 194805.56 194683.17 194714.75 198565.53 198510.95 198486.78 194873.44 194945.95 194878.91 194830.27 194813.55 194892.02 194949.58 194948.34 195355.23 195280.95 195375.91 195439.75 195463.13 195466.77 195371.86 195268.91 195000.91 195004.98 195003.69 195055.19 195117.95 195190.25 195240.05 195125.59 195310.91 195246.75 194901.66 195248.31 194805.48 194942.39 194738.95 195183.30 195132.95 194777.31 194410.23 194410.06 194413.63 195190.06 195159.05 195220.73 195149.45 195182.70 195245.34 195137.81 195197.16 195193.81 195252.33 195189.16 195133.50 195311.05 195317.94 195318.91 195306.66 195385.59 195306.89 195689.44 195711.52 195816.27 195688.81 195806.20 195740.95 195708.30 195860.77 195925.05 195983.13 195928.30 195877.59 195867.80 195739.16 195809.91 195614.31 195558.50 195180.03 195178.59 195258.48 195110.48 195148.02 195187.84 195199.91 195399.36 195436.00 195439.98 195958.31 195986.23 196040.97 195930.17 195762.25 195754.39 195743.41 195701.63 196041.02 195870.45 195821.73 195801.70 195557.73 195624.45 195561.13 195421.42 195392.61 195388.30 195498.36 195443.09 195448.SO 195325.41

COLLAR Iml

73.81 68.64 73.05 100.29 99.72 98.62 98.50 99.39 100.39 99.70 100.04 66.54 110.51 96.23 89.18 44.36 60.75 68.00 42.18 33.59 31.79 31.66 33.43 31.82 34.08 33.88 34.91 36.54 36.01 176.52 177.47 177.94 111.29 106.99 95.93 B7.39 44.07 46.80 73.82 92.90 143.64 142.38 139.45 135.37 129.88 118.25 145.76 143.02 113.49 106.49 100.57 101.92 93.16 80.13 64.80 125.07 50.72 101.31 63.14 82.91 62.67 86.82 50.65 76.40 65.05 61.77 77.38 BO. 39 71.44 143.03 143.42 147.50 142.79 144.98 148.64 140.07 130.70 127.16 119.23 122.14 130.35 96.35 135.53 125.16 116.40 126.75 99.13 34.97 30.09 39.69 53.38 48.29 53.28 52.71 55.61 53.42 51.29 40.21 40.77 35.12 35.08 45.69 31.85 27.47 38.42 77.86 69.00 59.42 60.35 59.81 55.40 125.26 147.73 139.50 66.74 61.21 68.27 62.45 52.89 15.83 56.43 53.81 80.54 51.05 33.41 33.92 36.30 43.88 19.99 37.89 25.73 34.89 45.10 73.49 84.90 74.08

DEPTOP (ml

17.23 10.60 28.05 31.09 24.80 19.20 20.22 24.75 35.42 34.47 31.34 16.15 32.35 34.10 28.10 3.60 11.76 24.80 31.11 31.92 24.83 21.96 30.00 18.74 18.71 31.82 32.55 18.55 29.98 32.96 33.67 32.82 58.27 55.86 18.35 11.21 39.11 37.18 26.30 17.48 48.63 40.65 16.22 11.85 12.75 25.00 52.99 12.62 64.93 58.26 50.85 58.12 52.92 45.53 34.35 72.15 27.69 57.79 18.30 46.14 25.80 41.27 10.69 41.86 31.22 51.73 96.35 85.19 105.29 44.24 45.41 48.76 45.41 16.19 50.08 57.86 50.55 55.83 17.17 57.79 70.11 51.07 52.70 47.55 41.39 54.85 44.85 20.54 10.15 19.65 46.77 49.83 48.88 64.93 59.40 37.99 30.29 17.48 22.90 11.18 13.40 37.20 30.70 27.80 50.25 10.44 33.27 22.71 27.46 30.39 29.94 59.70 74.75 71.45 52.19 43.12 45.33 50.63 47.92 40.55 57.88 48.22 68.88 39.24 10.05 10.56 39.88 41.67 53.40 37.45 22.66 40.11 50.66 80.08 90.46 68.13

DEPBOT (m) 24.58 13.68 34.52 37.78 31.31 25.72 26.55 31.34 41.98 41.00 37.45 25.15 39.50 41.18 35.59 4.45 19.22 28.40 37.17 38.72 31.26 29.48 36.06 20.32 25.88 39.20 39.45 25.67 36.02 3S.04 37.74 10.18 66.65 64.51 50.42 14.22 15.40 39.50 28.30 54.41 56.10 15.10 50.81 19.75 17.60 33.00 60.57 14.61 73.86 67.22 59.95 66.13 62.51 56.05 16.33 82.12 34.93 67.93 19.20 57.04 27.58 43.16 47.23 50.55 35.17 59.45 102.29 91.18 111.53 50.36 51.29 54.09 48.34 48.14 54.50 63.53 56.13 62.72 53.97 64.42 77.51 66.19 59.10 54.13 48.41 61.70 53.02 27.94 15.94 25.86 55.11 54.23 56.70 66.31 62.25 44.65 36.26 24.69 30.50 18.20 18.70 44.20 37.30 35.50 60.58 52.11 45.49 24.00 29.36 34.73 33.70 66.60 78.92 78.54 58.89 18.46 50.80 56.41 56.38 47.76 64.32 57.28 74.11 47.39 11.47 11.96 16.11 50.52 60.11 14.93 30.96 16.99 58.17 36.58 96.47 72.00

THICK TOPELEV BOTELEV Im) (m) (ml 7.35 56.58 49.23 3.08 58.04 54.96 6.47 45.00 38.53 6.35 69.20 62.51 6.51 74.92 68.41 6.52 79.42 72.90 5.16 78.28 71.95

6.24 6.56 6.15 6.11 9.00 7.15 7.08 7.49 0.85 7.46 3.60 6.06 6.80 6.43 7.52 6.06 1.58 7.11 7.38 S.90 7.12 6.01 2.08 1.07 7.36 9.38 8.29, 2.07 2.98 5.96 2.02 2.00 5.38 7.47 1.15 1.62 1.90 1.85 B.00 7.58 2.02 B.93 8.96 9.10 3.01 9.62 10.S2 11.56 9.97 7.24 10.14 0.90 10.90 1.78 1.89 6.54 8.69 3.95 7.72 5.63 5.99 6.21 6.12 5.88 5.33 2.51 1.95 1.42 5.67 5.58 6.89 6.19 6.63 7.10 12.12 6.40 6.58 7.02 6.85 8.17 7.40 5.79 6.21 8.31 1.35 7.82 1.38 2.85 6.66 5.97 6.40 7.60 6.72 5.30 6.60 5.60 6.90 10.33 11.34 12.22 1.29 1.90 4.34 3.76 5.70 4.17 7.09 6.70 5.34 1.97 5.39 7.95 7.21 6.44 9.06 5.23 8.15 1.42 1.40 6.S3 8.85 6.71 7.48 B.30 6.88 6.97 6.SO 6.01 3.87

74.64 64.97 65.23 68.70 50.39 78.16 62.13 61.08 40.76 48.99 13.20 11.07 1.67 6.96 9.70 3.43 13.08 15.34 2.06 2.36 17.99 6.03 143.56 143.80 145.12 53.02 51.13 47.58 16.15 1.63 9.32 17.52 15.12 95.01 101.73 93.23 90.52 87.13 93.25 92.77 100.40 49.56 48.23 49.72 43.80 10.24 31.60 30.15 52.92 23.03 13.52 11.81 36.77 36.87 15.55 9.96 31.51 33.83 10.01 -18.97 -4.80 -33.85 98.79 98.01 98.74 97.35 98.79 98.56 82.21 80.15 71.33 72.06 64.35 60.24 42.28 B2.83 77.61 75.01 71.90 54.28 14.43 19.94 20.04 6.61 -1.59 1.40 -12.22 -3.79 15.43 21.00 22.73 17.87 23.64 21.68 B.49 1.15 -0.33 38.17 37.42 35.73 36.71 32.89 29.42 25.46 65.56 72.98 68.05 14.55 18.09 22.44 11.82 1.97 5.28 -1.45 5.59 11.66 11.81 23.36 23.36 -3.58 2.21 -3.41 0.44 3.07 -5.22 -5.56 -6.59 -5.56 5.95

68.05 58.41 58.70 62.59 11.39 71.01 55.05 53.59 39.91 11.53 39.60 5.01 -S.13 0.53 2.18 -2.63 11.50 8.20 -5.32 -4.54 10.87 -0.01 141.48 139.73 137.76 44.64 42.48 45.51 43.17 -1.33 7.30 45.52 38.49 87.54 97.28 B8.61 BS.62

82.28 85.25 85.19 98.38 39.63 39.27 40.62 35.79 30.62 24.08 18.47 12.95 15.79 33.38 13.94 25.87 35.09 43.66 3.42 25.85 29.88 2.32 -21.91 -10.79 -40.09 92.67 92.13 93.41 94.45 96.84 94.14 76.54 74.57 64.44 65.26 57.72 52.84 30.16 76.43 71.03 67.99 65.05 46.11 7.03 14.15 13.83 -1.73 -5.94 -3.42 -13.60 -6.64 3.77 15.03 15.52 10.27 16.92 16.38 1.49 -5.45 -8.03 27.84 25.75 23.51 35.42 30.99 25.08 21.70 58.66 68.81 60.96 7.85 12.75 17.47 6.04 -3.49 -1.93 -7.89 -3.47 6.13 3.66

21.94 21.96 -10.11 -6.64 -10.12 -7.04 -5.23 -12.10 -13.07 -13.09 -11.57 2.08

DDH

R5359 R5360 R5361 R5362 R5363 R5364 R5365 R5366 R5371 R5372 R5373 S5374 R5377 R5378 R5384 R5385 RS386 R5387 R5390 R5391 R5392 R5393 R5394 R5396 R5398 R5399 R5400 R5401 R5402 R5403 R5404 R5405 R5407 RS408 R5409 R5411 R5412 R5413 R5411 R5415 R5416 R5417 R5418 R5419 R5420 R5421 R5422 R5423 R5421 R5426 R5427 RS42S R5432 R5434 R5435 R5436 R5437 R5438 R5439 R5441 R5442 R5443 R5444 RS445 K5446 R5447 R5448 R5450 R5451 R5453 R54 55 R5459 R5460 R5461 R5462 R5464 R5465 R5466 RS467 RS468 R5470 R5471 R5472 R5473 RS474 R5475 R5477 R5479 R5480 R5481 R5505 R5506 R5507 R5508 R5509 R5510 R5511 R5512 R5513 R5514 R5516 R5517 R5518 R5519 R5522 RS523 R5524 R5526 R5527 R5529 R5530 R5534 R5538 R5539 R5541 R5542 R5543 R5544 R5546 R5547 R5548 R5549 R5550 R5551 R5552 R5553 R5554 R5555 R55S6 R5557 R5558 RSSS9 R5560 R5561 R5562 R5563

EASTING (m)

97992.69 98073.47 98056.86 98125.17 98064.67 98098.10 98005.67 98065.18 97967.24 97952.40 97944.15 97918.12 97920.39 97961.24 98198.29 98282.77 98303.83 98269.98 98326.71

98328.92 98355.73 98321.97 98355.22 98330.01 98354.77 98374.11 98391.97 98391.21 98281.49 98172.58 98165.60 98136.34 98150.50 98215.96 98202.81 98160.12 98100.64 98124.14 98287.85 98358.85 98380.84 98311.90 98349.11 98379.31 98332.67 98360.51 98374.72 98391.35 98355.81 98427.34 98439.64 98156.42 98126.19 98089.43 98086.82 98008.86 98022.90 98080.81 93156.66 98093.55 98083.58 98033.56 98008.31 97918.44 97936.71 97907.62 97909.06 97901.91 97922.58 97942.75 98151.26 98032.64 98024.01 98032.60 98048.24 97927.56 97915.43 97903.53 97939.72 97931.63 98085.72 97970.72 98049.57 98158.45 98129.35 98099.66 98304.24 98234.19 98262.22 98318.73 98131.64 98071.28 98003.42 97576.36 97511.98 97435.69 97495.81 97451.37 97352.36 97579.05 98496.25 98550.01 98498.64 98431.51 984 56.20 98355.58 98226.55 98138.99 98362.27 98370.80 98339.95 98409.09 98551.28 98512.88 97675.21 97463.14 97545.20 97536.99 97981.18 98023.36 98069.35 97946.51 98081.64 97865.78 97932.68 98027.24 98206.31 97670.20 97613.79 98150.36 98202.01 97675.91 98067.15 98218.80 98144.88 98257.98

NORTHING (m)

195184.78 195113.66 195176.77 195181.41 195221.98 195050.73 195343.63 195442.44 196003.45 195958.81 195924.73 195788.94 195525.33 195493.27 195857.73 195582.95 195850.09 195893.44 195847.03 195807.95 195789.91 195733.94 195736.58 195690.88 195687.42 195619.23 195624.33 195653.05 195780.88 195628.84 195535.45 195562.95 195701.81 195645.80 195443.33 195399.64 195502.30 195631.70 195693.50 195806.06 195805.44 195636.92 195853.44 195851.16 195895.48 195906.67 195966.20 195951.52 195938.27 195953.16 195970.88 195655.98 195902.67 196137.31 196188.11 196171.70 196114.70 196059.22 195940.91 195677.06 195632.11 195505.22 195500.84 195671.44 195662.80 195631.80 195557.45 195528.78 195486.33 195399.48 195188.98 195260.17 195309.20 195355.45 195692.19 195865.98 196007.30 196044.22 196100.72 196181.58 195967.77 195838.97 195832.63 195024.02 195037.63 195077.17 195718.02 195668.63 195691.08 195688.03 194564.31 194577.86 194578.08 194806.59 194758.11 194695.09 194803.80 194793.27 194793.27 194699.98 194460.28 194487.56 194500.78 194463.14 194433.92 194292.66 194338.44 194325.27 194722.50 194751.34 194721.66 194702.19 194544.72 194571.19 194701.45 194895.66 194620.72 194547.55 194821.41 194822.42 194856.88 194876.03 194801.20 194885.88 194813.91 194740.81 194679.78 194625.03 194561.88 194770.22 194773.45 194561.44 194683.20 194569.56 194666.11 194780.73

COLLAR Iml

62.57 60.40 49.08 41.29 37.80 44.98 35.28 44.54 79.61 78.09 79.16 67.67 52.21 61.68 36.75 19.73 50.70 52.93 56.23 60.36 63.48 56.15 59.27 57.47 59.28 66.45 67.71 67.11 49.55 38.28 43.96 35.14 29.37 39.12 42.78 42.74 29.78 25.79 53.80 63.90 64.57 54.07 56.77 60.49 61.88 66.64 67.75 73.44 62.60 79.96 79.96 34.30 29.50 38.83 47.14 46.23 45.34 40.90 29.33 31.57 32.64 27.31 37.03 41.90 11.05 17.67 57.93 59.76 65.78 74.10 39.14 28.70 27.83 30.58 47.31 73.65 B8.12 90.61 B9.16 79.71 12.91 55.80 13.41 31.36 33.43 44.45 55.14 51.72 16.01 56.91 99.22 99.38 98.63 87.03 70.76 44.61 65.99 56.22 56.22 87.10 54.21 53.24 68.15 64.53 55.80 70.96 78.75 75.29 44.08 40.53 47.29 15.32 15.99 50.36 104.09 70.64 59.05 76.43 116.82 103.37 94.10 106.57 91.21 126.21 120.43 110.85 78.99 88.96 B9.55 71.89 62.60 88.08 106.26 104.82 87.88 51.13

DEPTOP Im)

44.83 47.24 23.95 13.67 B.75 35.24 13.85 52.66 67.72 68.34 84 .90 54.80 56.92 70.80 12.25 16.90 18.50 16.50 28.10 38.40 37.28 27.80 35.32 35.55 34.23 30.66 11.00 15.86 9.88 21.45 29.18 25.56 9.40 20.10 34.90 38.70 28.50 12.82 11.50 36.85 30.92 19.45 33.62 29.14 36.32 34.54 32.70 28.68 30.66 34.87 33.33 16.70 5.57 2.00 10.62 21.11 20.50 10.60 9.26 16.32 19.86 31.12 12.31 50.23 37.26 61.67 65.70 70.08 73.81 82.08 10.22 10.71 35.17 32.27 36.31 103.17 83.56 87.10 79.71 66.10 17.61 65.53 29.32 20.70 21.03 31.60 11.70 13.72 10.19 37.57 101.43 101.21 99.18 34.83 72.47 33.25 64.20 53.73 46.18 93.08 122.43 39.70 85.91 75.00 89.25 143.24 100.63 84.46 25.59 30.34 33.91 39.28 54.58 43.02 109.62 71.12 41.19 38.15 130.50 115.25 101.76 120.95 100.90 139.52 135.77 120.62 78.10 90.54 68.76 76.28 62.18 75.77 114.70 100.16 91.22 16.38

DEPBOT Im) 16.78 19.73 29.58 16.31 11.83 10.39 50 .31 58 .63 73 .23 74 .79 85 .80 56 .65 62.53 78 .41 15.40 17.00 25.44 17.00 31.31 11.91 13.03 28.62 10.02 11.12 11.12 39.70 12.00 13.90 11.67 27.18 36.60 31.71 11.70 20.95 13.60 19.00 37.38 19.91 11.70 12.20 38.86 22.90 35.98 35.01 38.34 38.67 34.06 37.93 31.53 11.88 39.51 22.32 10.82 3.71 12.15 25.28 21.12 16.59 9.52 21.07 27.82 39.38 50.06 53.26 16.01 62.01 70.06 71.88 78.18 88.70 13.35 11.16 13.19 11.51 13.91 101.31 90.07 91.91 83.81 70.03 24.30 66.87 36.71 24.40 27.46 35.92 12.91 14.88 11.54 40.69 111.77 111.15 108.41 95.93 B2.78 11.93 75.11 64.25 50.08 102.52 131.09 44.86 93.50 38.50 92.53 144.00 107.79 98.67 32.21 38.87 43.19 40.95 51.16 49.75 119.47 77.06 50.21 15.30 138.70 122.87 108.72 128.40 107.62 148.00 144.81 129.62 85.63 98.94 76.37 33.40 69.10 33.79 124.46 109.67 99.82 53.13

THICK Im) 1.95 2.27 5.09 2.26 3.08 4.72 6.46 5.45 5 .51 6.45 0.90 1.30 5 .61 7.05 0.60 0.10 3.40 0.50 2.37 2.28 5.36 0.82 4.70 1.72 6.21 9.04 1.00 3.04 1.53 5.73 7.42 5.88 2.30 0.85 8.70 9.40 8.88 7.09 2.50 5.3S 7.47 1.53 2.36 5.90 2.02 1.13 1.36 7.22 0.87 7.01 6.18 5.62 5.25 1.71 1.09 1.17 3.62 5.99 0.26 7.75 6.66 7.11 6.84 2.78 8.78 0.34 4.36 1.80 4.34 6.62 2.70 0.42 7.83 7.35 6.90 0.87 6.51 7.54 1.13 3.93 6.17 1.31 7.39 3.70 2.61 1.32 0.85 1.16 1.35 2.94 10.34 9.91 9.26 10.24 9.98 8.14 9.35 10.20 3.90 9.44 8.66 5.16 7.59 13.50 3.28 0.76 7 .04 6.01 6.62 8.53 9.25 1.67 6.58 6.73 9.44 5.94 8 .90 7.15 8.20 7.62 6.94 7.45 6.36 8.18 9.07 9.00 7.53 8.40 7.61 7.12 6.92 8.02 9.76 8.82 8.60 6.75

TOPELEV (ml

17.71 13.16 25.13 27.62 29.05 9.71 -8 .57 -8 .12 11.89 9.75 -5 .71 12 .87 -4 .68 -6 .12 26.50 32.83 32.20 36.43 28.13 21.96 26.20 28.35 23.95 21.92 25.05 35.79 26.71 21.25 39.67 16.83 14.78 9.58 19.97 19.02 7.88 1.01 1.28 12.97 12.30 27.05 33.65 31.62 23.15 31.35 25.56 32.10 35.05 11.76 31.94 45.09 16.63 17.60 23.93 36.83 36.52 25.12 21.81 30.30 20.07 15.25 12.78 -1.11 -5.28 -8.33 3.79 -11.00 -7.77 -10.32 -8.06 -7.98 28.92 17.96 -7.29 -1.69 11.03 -29.82 1.86 3.21 9.75 13.61 25.30 -9.73 14.09 10.66 9.10 12.85 13.44 38.00 35.82 19.34 -2.21 -1.83 -0.55 2.20 -1.71 11.36 1.79 2.49 10.01 -5.98 -68.22 13.54 -17.76 -10.47 -33.45 -72.28 -21.88 -9.17 18.49 10.19 13 .35 6.04 -8 .60 7.34 -5 .53 -0.48 17.86 38 .28 -13.68 -11.88 -7.68 -14.38 -9 .69 -13.31 -15.34 -9 .77 0.89 -1.58 20.79 -4.39 0.42 12.31 -8.44 4.36 -3.34 4.75

BOTELEV Im)

15.79 10.67 19.50 24.48 25.97 4.59 -15 .03 -14.09 6.38 3.30 -6.64 11.02 -10.29 -13.73 23.35 32.73 25.26 35.93 24.69 18.12 20.15 27.53 19.25 16.35 17.86 26.75 25.71 18.21 31.88 11.10 7.36 3.10 17.67 18.17 -0.82 -6.26 -7.60 5.88 39.10 21.70 25.71 31.17 20.79 25.15 23.54 27.97 33.69 35.51 31.07 38.08 10.45 11.98 18.68 35.09 34.99 20.95 21.22 24.31 19.81 7.50 1.82 -12.07 -13.03 -11.36 -1.99 -14.34 -12.13 -12.12 -12.40 -14.60 25.79 17.54 -15.31 -13.93 3.40 -30.69 -1.65 -4.33 5.62 9.68 18.61 -11.07 6.70 6.96 5.97 8.53 12.23 36.84 34.47 16.22 -12.55 -11.77 -9.81 -8.90 -12.02 2.68 -9.15 -8.03 6.14 -15.42 -76.88 B.38 -25.35 -23.97 -36.73 -73.04 -29.04 -23.38 11.87 1.66 4.10 4.37 -15.18 0.61 -15.38 -6.42 B.84 31.13 -21.88 -19.50 -14.62 -21.83 -16.41 -21.79 -24.41 -18.77 -6.64 -9.98 13.18 -11.51 -6.50 1.29 -18.20 -1.85 -11.91 -2.00

Appendix 6.5 (confd)

DDH

R5564 RS566 R5571 R5702 R5703 R5704 R5720 R5721 R5738 R5742 R5749 RS750 R5753 RS754 R5787 R5793 R5795 R5805 RS814 R5826 R5836 R5845 R5846 R5848 R5852 R5879 R5963 R5964 R5965 R5966 R5967 R5968 R5969 R5970 R5971 R5972 R5973 R5974 R5975 R5976 R5977 R5978 R5979 R5980 S5983 R5982 RS983 R5985 R5986 R5987 RS988 R5989 R5992 R5993 RS994 R5995 R5996 R5998 R5999 K6004 R6005 R6009 R6010 R601S R6024 R6158 R6161 R6167 R6176 R6200 R6201 R6202 R6203 R6204 R6205 R6207 R6208 R6209 R6210 R6212 R6213 R6214 R6215 R6216 R6217 R6218 R6232 R6233 R6234 R6239 R6240 R6241 R6242 R6245 R62S0 R6251 R6253 R6288 R6289 R6313 R6315 R6316 R6317 R6320 R6376 R6380 R6381 R6382 R6486 R6487 R6488 R6190 R6666 R6678 R6686 R6689 R6691 R6692 R6693 R6694 R6695 R6696 R6697 R6698 R6699 R6780 R6781 R6782 R6783 R6785 R6786 R6787 R6788 R6790 R6791 R6792

EASTING Im)

98203.28 98070.11 97881.02 95425.82 95135.68 95275.32 95288.44 95284.60 95621.72 96088.05 95845.21 95845.20 95543.71 95411.42 94766.08 94681.48 94569.08 94512.00 94414.93 94353.36 94091.01 94574.01 94469.84 94258.18 93979.33 95165.85 99174.47 99224.58 99184.98 99133.63 99134.22 99124.07

99059.03 99004.19 98954.78 99878.85 98911.01 99051.92 99001.45 98950.69 99059.06 99056.33 99001.64 99000.08 99008.39 98945.04 98932.12 98880.85 98853.73 98931.70 98816.92 98750.37 98762.64 98926.78 98934.15 98810.32 98758.46 98626.72 98625.20 95538.82 95576.96 95253.94 95248.01 94936.25 94666.88 95009.02 94715.23 94485.73 94249.10 98813.78 98792.75 98817.06 98764.12 98627.49 98611.75 99002.76 98949.63 99113.11 99056.43 99200.60 98907.42 98777.85 98850.64 98889.81 99126.53 99287.61 99353.15 99567.62 99564.26 99505.60 99508.06 99445.75 99389.03 99253.60 99323.90 99259.38 99307.04 97951.47 97970.87 100482.82 100235.43 99985.02 99998.05 99755.55 101145.03 101128.38 101365.98 101634.92 95998.61 95992.91 96017.02 96012.42 96731.86 96502.23 96315.28 96381.62 96304.39 96312.25 96375.43 96438.18 96254.32 96183.93 96175.37 96149.45 96120.67 97573.88 97628.45 97613.48 97623.41 97556.24 97566.09 97544.19 97544.30 97762.25 97823.52 97636.50

NORTHING (ml

194808.30 194437.34 194403.81 196136.92 196493.19 196504.88 196190.09 196260.78 196014.13 195885.44 195880.25 195880.25 195966.52 196003.95 196809.80 197022.23 197324.34 197500.00 197731.30 197946.09 198149.14 198272.03 198366.95 198350.11 198422.97 196019.27 199190.41 199302.69 199131.34 199242.33 199179.88 199130.02 199127.06 199118.55 199121.84 199124.55 199170.78 199057.61 199062.56 199059.52 199196.02 199242.20 199183.41 199243.91 199317.63 199296.98 199239.67 199082.69 199033.53 198968.69 198987.53 198987.38 199126.48 198923.59 198858.20 198930.61 198935.58 198949.31 199034.30 196181.94 196153.34 196211.89 196264.20 196617.31 196805.20 196369.09 196587.05 196703.38 197369.56 199034.94 198993.05 199179.38 199232.16 199240.77 199153.77 199359.19 199413.25 199356.69 199374.16 199362.41 199110.08 199078.45 199089.80 199194.88 199302.19 199204.97 199389.06 199440.53 199500.73 199455.30 199506.77 199560.92 199576.30 199572.05 199455.33 199439.55 199595.55 195345.95 195332.44 194684.86 194697.69 194770.94 195014.16 194994.86 194250.23 194021.31 194000.52 194000.45 195312.77 195331.39 195366.13 195281.16 196147.70 195855.72 196190.91 195626.08 195572.59 195509.48 195452.09 195445.02 195567.19 195498.52 195564.88 195624.03 195568.44 194462.38 194406.38 194324.03 194284.38 194324.20 194368.06 194395.09 194454.30 194415.16 194283.89 194433.89

COLLAR (ml

57.35 89.56 84.74 95.71 37.77 53.54 74.78 68.44 65.07 90.05 52.23 52.23 78.50 77.67 86.00 B3.37 80.30 75.00 38.18 30.98 28.34 27.66 50.03 65.48 43.65 85.39 146.32 149.30 140.53 137.32 132.17 130.99 122.88 122.71 122.56 136.52 137.36 127.57 121.43 121.52 133.92 140.12 135.54 137.06 149.47 151.53 141.37 125.41 119.22 125.96 116.95 116.95 140.83 132.08 142.51 119.86 111.77 125.30 135.38 102.90 94.78 63.71 60.88 47.50 91.32 26.81 50.90 100.07 51.88 115.73 116.13 158.51 169.49 174.98 156.50 154.69 169.94 161.16 162.95 152.54 129.37 133.22 132.60 146.90 143.23 151.28 174.52 216.66 219.96 204.90 205.96 202.95 203.76 202.52 175.95 172.51 200.49 65.37 55.90 26.01 25.67 47.87 42.65 74.31 50.31 69.72 20.13 29.36 141.80 140.56 128.83 142.79 96.08 107.15 126.24 132.16 144.74 140.28 135.72 134.21 134.72 125.49 111.00 103.27 105.69 50.58 49.73 50.11 50.00 18.85 50.76 50.69 19.90 62.11 57.87 50.99

DEPTOP Iml

56.16 70.68 69.58 84 .08 60.00 93.89 46.76 51.57 67.35 108.90 52.72 19.85 43.79 37.93 85.67 93.60 111.20 114.42 94.96 105.78 107.01 175.90 197.27 177.41 112.70 2.53 23.47 10.36 14.92 28.17 17.20 16.14 11.05 16.42 23.66 51.91 50.50 11.36 13.55 23.25 32.06 36.41 37.21 15.75 53.66 70.88 62.68 11.26 39.60 31.02 15.23 74.35 103.31 46.64 63.40 52.92 52.31 93.37 106.70 102.70 95.09 38.21 37.60 57.28 74.00 14.96 23.66 36.78 32.00 45.37 50.78 110.30 133.52 168.12 143.92 60.41 89.84 48.18 60.98 18.99 39.13 79.74 55.07 65.97 29.86 7.24 12.40 11.42 1.00 1.00 0.00 12.14 27.92 35.47 19.93 20.26 49.80 76.12 66.34 18.18 38.38 79.10 19.68 31.83 69.61 144.92 67.96 38.44 29.41 27.62 42.37 32.21 154.18 157.25 192.79 95.42 91.34 79.30 73.32 74.60 75.08 47.00 39.08 41.88 28.80 7.51 11.31 10.02 14.89 20.52 17.13 7.18 7.28 43.52 56.43 17.90

DEPBOT (m) 62.64 76.33 74.66 84.60 61.80 95.87 48.19 52.22 70.46 110.63 57.30 50.10 46.37 40.40 87.35 94.76 112.73 115.82 96.45 107.22 103.35 177.22 197.50 178.13 113.04 1.76 29.70 15.47 21.29 34.59 23.50 23.18 18.52 23.81 29.39 54.38 52.35 17.00 19.04 26.25 38.76 50.28 11.32 53.02 59.13 77.49 74.06 45.02 44.25 38.09 19.58 75.50 109.25 53.55 69.28 60.69 60.44 96.86 111.93 103.44 95.87 39.61 38.88 58.82 76.00 16.62 24.85 37.90 33.02 19.21 61.10 116.51 110.69 176.72 160.22 63.16 90.77 51.86 64.92 24.48 42.79 94.84 57.04 68.70 37.56 11.22 14.25 12.52 3.75 3.16 3.60 14.92 29.94 41.19 22.81 25.46 54.96 81.82 71.79 20.30 39.95 80.96 21.65 83.89 70.56 145.95 68.85 39.31 32.50 29.90 19.20 36.31 163.00 169.50 202.80 100.30 98.91 B6.47 B0.6S 32.02 32.57 54.65 17.92 46.82 33.84 15.16 21.21 11.12 16.04 23.09 20.15 10.65 8.55 49.95 62.81 26.51

THICK Im) 6.48 5.65 6.08 0.52 1.69 1.50 1.43 0.65 3.11 1.73 1.58 0.55 2.58 2.17 1.68 1.16 1.53 1.10 1.19 1.11 1.31 1.32 0.23 0.72 0.31 2.23 6.23 5.11 6.37 6.12 6.30 7.04 7.47 6.13 5.72 2.47 1.8S 5.20 5.15 3.00 6.70 7.37 6.77 7.27 3.71 6.61 7.99 2.51 3.69 1.07 1.35 1.15 5.91 6.91 5.88 7.77 7.72 3.19 1.15 0.71 0.78 1.10 1.28 1.51 2.00 1.66 1.19 1.12 1.02 3.47 10.20 6.21 7.17 B .60 1.71 2.71 0.93 3.68 3.91 5.49 3.66 8.31 1.97 2.73 7.70 3.98 1.85 1.10 2.75 2.16 3.60 2.78 1.92 5.15 2.91 5.20 1.54 5.70 5.15 2.12 1.57 1.86 1.97 2.06 0.95 1.03 0.89 0.B7 3.09 2.28 6.83 1.10 8.82 12.25 10.01 1.88 7.22 7.17 7.33 7.06 6.76 7.19 8.13 1.91 5.01 7.65 9.51 1.10 1.15 2.57 3.02 3.17 1.27 6.13 6.38 3.61

TOPELEV Im)

1.19 18.88 16.16 11.63 -22.23 -40.35 28.02 16.87 -2.28 -16.85 -0.49 2.38 34.71 39.74 0.33 -10.23 -30.90 -39.42 -56.78 -74.80 -78.70 -148.2 -147.2 -111.9 -69.05 82.86 122.85 138.94 125.61 109.15 114.97 114.85 111.83 106.29 98.90 84.61 87.36 116.21 107.88 98.27 101.86 103.68 98.33 91.31 95.81 80.65 78.69 84.15 79.62 91.94 71.72 42.60 37.52 85.44 79.11 66.94 59.46 31.93 28.68 0.20 -0.31 25.47 23.28 -9.78 17.32 11.85 27.24 63.29 19.38 70.36 65.35 48.21 35.97 6.86 12.58 91.28 80.10 112.98 101.97 133.55 90.21 53.48 77.53 80.93 113.37 144.01 162.12 205.24 218.96 203.90 205.96 190.83 175.81 167.05 156.02 152,25 150.69 -10.75 -10.11 7.83 -12.71 -31.23 22.97 -7.52 -19,30 -75.20 -17.83 -9.08 112.39 112.91 B6.46 110.56 -58.10 -50,10 -66.55 36.74 53.40 60.98 62.40 59.61 59.64 78.49 71.92 61.39 76.89 13.07 38.42 40.12 35.11

28.33 33.63 43.51 42.62 18.62 1.41 33.09

BOTELEV

(m) -5.29 13.23 10.08 11.11 -24.03 -42.33 26.59 16.22 -5.39 -20.58 -5.07 1.83 32.13 37.27 -1.35 -11.39 -32.43 -40.82 -58.27 -76.24 -80.01 -149.56 -147.47 -112.65 -69.39 80.63 116.62 133.83 119.21 102.73 108.67 107.81 104.36 98.90 93.18 82.14 85.51 110.57 102.39 95.27 95.16 89.84 91.22 94.04 90.34 74.04 67.31 30.39 74.97 87.87 67.37 11.15 31.58 78.53 73.23 59.17 51.33 28.44 23.45 -0.54 -1.09 24.07 22.00 -11.32 15.32 10.19 26.05 62.17 18.96 66.52 54.73 41.97 28.80 -1.74 -3.72 91.23 79.17 109.30 98.03 128.06 B6.58 38.38 75.56 78.20 105.67 140.06 160.27 204.11 216.21 201.74 202.36 188.03 173.92 161.03 153.11 147.05 145.53 -16.45 -15.89 5.71 -14.28 -33.09 21.00 -9.58 -20.25 -76.23 -48.72 -9.95 109.30 110.66 79.63 106.48 -66.92 -62.35 -76.56 31.86 45.80 53.81 55.07 52.19 52.15 70.84 63.08 56.45 71.85 35.12 28.52 39.02 33.96 25.76 30.61 10.01 11.35 12.19 -4.94 24.48

DDH

R6793 R6794 R6795 R6797 R6798 R6799 R6911 R6912 R6913 R6914 R6917 R6926 R6931 R6936 R6940 R6948 R6961 R6962 R6963 R6964 R6965 R6966 R6967 R6968 R6969 R6970 R6972 R6974 R6975 R6976 R6977 R6978 R6979 R6980 R6981 R6983 R6984 R7047 R7048 R7053 R7055 R7057 R7059 R7061 R7062 R7501 R7502 R7503 R7504 R7505 R7506 R7507 R7508 R7509 R7510 R7511 R7512 R7513 R7535 R7536 R7537 R7538 R7539 R7540 R7542 R7543 R7544 R7545 R7546 R7547 R7548 R7549 R7550 R7551 R7552 R7553 R7554 R7555 R7556 R7557 R7558 R7559 R7560 R7561 R7562 R7563 R7565 R7566 R7567 R7568 R7569 R7570 R7571 R7574 R7575 R7576 R7578 R7581 R7582 R7583 R7584 R7587 R7S88 R7592 R7593 R7594 R759S R7596 R7597 R7598 R7599 R7600 R7601 R7602 R7603 R7604 R7605 R7607 R7610 R7611 R7612 R7650 R7651 R7653 R7654 R7656 R7657 R76S8 R7666 R7678 R7686 R7688 R7689 R7690 R7691 R7692

EASTING (ml

97618.78 97603.18 97588.08 97673.59 97645.92 97703.73 99190.27 99194.75 99113.89 99113.46 99118.33 98998.49 99056.69 99102.82 98991.18 99220.81 98053.88 98102.65 98175.73 98171.14 98158.49 98165.58 98080.74 97975.43 97926.90 97913.62 98093.71 98190.96 98255.98 97766.86 97921.41 96281.83 98313.02 98020.44 97917.81 98433.51 98433.56 92874.81 93777.81 93579.99 93388.30 93229.79 94125.39 93507.61 93530.86 96061.43 96064.23 96045.61 96026.63 96148.20 96204.56 96270.54 96489.25 96547.56 96594.45 96540.20 96660.90 96560.70 96482.38 96584.88 96508.18 96643.99 96640.77 96755.61 96895.29 96899.29 96833.03 96951.40 97006.04 96875.86 96924.53 96864.59 96858.13 96926.40 96872.18 96811.02 96691.87 96760.97 96633.99 96682.07 96864.02 96863.17 96942.15 96934.64 96924.78 96867.27 96984.83 96819.70 96765.96 96686.70 96662.08 96726.88 96765.06 95960.90 95960.20 95992.83 95958.24 95978.48 95997.17 96012.68 95990.52 95985.06 96009.79 97043.25 97016.09 96976.06 96974.67 97937.47 97950.02 98000.64 98013.33 9770S.17 97711.34 97669.78 97648.98 97823.34 97837.10 97901.15 97881.13 97944.22 97995.96 100689.75 100711.55 100641.25 100655.44 100482.7.0 100465.79 100410.92 100482.63 100222.88 100502.07 100241.68 100102.20 100100.17 100088.08 99959.22

NORTHING Im)

194474.69 194554.34 194599.13 194358.42 194344.33 194334.66 195376.31 195442.47 195321.09 195271.44 195394.47 195260.23 195254.41 195486.47 195123.09 195072.58 196874.88 196941.61 196945.27 197011.56 196875.75 196759.55 196755.63 196808.88 196815.31 196751.28 196624.23 196608.72 196610.45 196594.38 196626.33 196902.38 196778.95 196967.59 196882.08 196657.80 196754.44 199588.44 198383.73 197850.19 198419.89 198822.91 197686.42 199056.36 198751.88 195563.30 195630.02 195685.83 195687.53 195674.63 195689.45 195692.20 195449.88 195455.81 195453.83 195381.55 195385.48 195503.66 195562.27 195565.70 195614.34 195627.05 195551.20 195600.28 195513.47 195574.22 195568.03 195578.80 195564.69 195031.75 195000.69 194968.59 194910.09 194900.09 194885.13 194890.13 194972.05 194969.31 195036.22 195061.19 194921.42 194946.92 194980.27 195032.55 195053.81 194997.55 194949.98 195321.59 195312.72 195333.06 195437.63 195447.23 195146.53 195272.91 195311.83 195362.69 195367.77 195452.94 195425.39 195405.59 195464.20 195383.58 195375.00 195072.02 195152.09 195259.05 195288.66 195499.92 194440.63 194439.05 194489.63 194293.00 194240.16 194308.61 194210.11 194951.19 195008.91 195041.80 194939.50 194960.27 195935.31 194439.66 194494.94 194433.52 194496.30 194501.81 194441.38 194509.09 194959.98 195130.38 194732.63 194890.77 194901.03 195159.73 195027.36 195040.48

COLLAR DEPTOP DEPBOT (m) (ml

50.55 17.02 50.89 27.26 50.71 35.13 50.19 16.21 50.36 12.02 50.45 24.47 151.27 6.12 158.74 0.00 127.63 0.00 126.42 3.40 133.70 3.26 98.86 3.00 115.27 4.59 140.80 0.00 80.82 15.71 89.99 22.57 199.58 206.87 193.48 191.61 174.25 169.52 175.79 171.27 166.34 167.05 170.65 165.00 189.27 191.28 190.31 205.20 181.65 198.45 172.25 190.48 164.63 137.90 157.00 123.01 134.20 106.00 135.55 149.40 148.63 163.84 126.81 102.91 135.46 110.48 188.40 195.17 187.35 207.00 62.65 10.14 67.49 14.73 73.32 186.95 51.65 106.09 64.29 57.90 83.29 74.34 49.86 53.87 18.33 14.74 36.65 133.43 31.42 136.25 97.48 14.50 88.92 14.62 78.39 13.90 77.51 7.71 91.02 42.60 100.44 62.74 121.14 86.50 130.69 76.12 119.16 73.95 109.29 70.00 112.99 70.06 B4.41 46.24 120.59 82.32 126.20 86.98 114.82 83.08 113.79 91.27 103.37 91.23 108.50 83.86 98.08 93.13 70.36 67.00 68.65 68.00 75.57 65.92 62.62 69.34 48.69 53.50 87.30 39.51 86.72 43.73 89.04 38.82 91.80 41.15 88.37 40.44 37.68 37.22 B8.72 37.86 101.02 50.57 97.30 47.51 105.01 53.79 100.68 53.02 90.92 40.62 90.30 40.33 33.44 36.07 34.32 42.66 81.13 39.90 38.09 38.33 64.75 18.12 60.61 29.41 67.29 32.56 B0.91 42.36 34.97 48.22 B2.55 50.05 78.03 48.95 159.01 45.06 118.39 33.09 134.61 19.04 137.67 18.43 109.67 11.20 113.63 12.40 117.03 9.30 107.49 7.50 127.91 13.20 128.01 12.42 13.21 23.94 37.54 5.61 53.85 30.23 48.39 29.35 70.37 55.91 69.98 51.38 71.05 50.39 71.49 57.51 50.30 30.07 50.39 66.83 49.69 20.64 50.35 19.43 133.10 137.43 124.76 120.73 110.97 106.54 116.68 129.51 101.20 117.59 89.36 99.64 27.20 56.18 19.33 33.80 16.64 53.28 17.19 37.74 17.61 47.11 17.31 60.44 24.25 62.23 40.67 3.65 90.33 3.65 34.13 14.66 57.10 27.35 34.93 19.97 75.54 5.74 48.26 28.91 44.09 20.88

(ml 24.68 34.78 43.08 21.60 17.28 30.15 6.80 2.00 2.00 4.30 6.30 4.46 10.84 2.00 16.34 28.50 215.70 202.40 176.41 177.59 174.54 172.89 198.55 212.37 205.23 199.47 155.69 124.93 113.86 154.75 172.04 109.56 118.69 202.26 215.00 15.32 15.04 191.48 107.38 61.19 75.08 55.15 15.37 135.15 137.64 16.10 19.92 18.68 11.42 47.81 67.90 95.22 84.43 83.07 82.36 79.66 60.76 92.62 94.66 95.90 101.20 103.11 93.59 101.85 74.56 80.02 74.64 71.15 54.75 50.13 ' 16.91 17.10 18.22 11.22 14.43 44.89 58.51 56.34 63.18 61.52 48.52 48.26 42.37 48.12 46.11 18.06 19.43 42.27 44.85 54.66 62.42 60.40 58.00 47.62 34.57 21 .68 20.23 11.75 12.80 9.90 8.65 14 .42 19.08 24.94 6.66 36.62 35.85 65.57 57.12 56.20 76.43 35.73 75.53 26.48 20.80 144.49 127.40 114.76 137.87 124.41 107.04 57.14 35.05 54.69 38.90 49.09 63.55 64.25 6.65 5.25 16.44 29.23 21.99 7.63 34.40 22.90

THICK

Im) 7.66 7.52 7.95 5.39 5.26 5.22 0.68 2.00 2.00 0.90 2.53 0.98 6.25 2.00 0.63 5.70 3.83 10.79 6.92 6.07 7.49 7.89 7.27 7.17 6.78 8.99 6.08 1.92 7.86 3.38 7.74 6.65 3.21 6.50 8.00 5.18 0.33 4.53 1.11 3.29 0.74 1.28 0.63 1.72 1.39 1.60 5.30 4.78 3.71 5.24 5.16 8.18 8.31 9.12 12.36 9.60 14.51 10.30 7.13 12.82 9.93 10.33 9.23 8.28 7.56 10.60 8.72 1.81 1.25 10.60 2.69 8.28 5.86 0.78 6.65 6.72 7.91 8.37 8.91 8.50 7.55 7.93 5 .28 1.62 5.30 9 .73 1.31 12.16 11.43 12.30 13.39 9.86 9 .05 2 .56 I .46 2 .10 1 .80 0.55 0 .40 0.60 1.15 1.22 6.66 1.00 2.59 6.06 6.50 7.59 5.74 5.81 11.92 5.66 8.70 5.84 1.37 7.08 6.67 3.22 8.36 6.85 7.40 0.96 1.25 1.41 1.16 1.98 1.84 2.02 3.00 1.60 1.78 1.88 2.01 1.89 5.49 2.02

TOPELEV BOTELEV

Im) 33.53 23.63 15.58 33.98 38.36 25.96 145.15 158.74 127.63 123.02 130.44 95.86 110.68 140.80 65.11 67.42 -7.29 1.87 4.73 4.52 -0.71 5.65 -2.01 -14.89 -16.80 -18.23 26.73 33.99 28.20 -13.85 -15.21 23.90 24.98 -6.77 -19.65 52.51 52.76 -113.6 -54.44 6.39 6.95 -4.01 3.59 -96.78 -54.83 32.98 74.30 64.49 69.80 48.42 37.70 34.64 54.57 4S.21 39.29 42.93 38.17 38.27 39.22 31.74 22.52 12.14 24.64 1.95 3.36 0.65 9.65 -6.72 -4.81 17.79 42.99 50.22 SO.65 47.93 50.46 50.86 50.45 49.79 51.22 47.66 50.30 49.97 47.37 41.66 41 .23 49 .76 46.63 31.20 34.73 38 .55 36.75 32 .50 29 .08 113.95 115.09 115.57 119.24 98 .47 101.23 107.73 99 .99 114 .71 115.59 19.27 31.93 23.62 19.04 14.43 18.60 20.66 13.98 20.22 -16.44 29.05 30.92 -4.31 4.03 4.43 -12.83 -16.39 -10.28 -28.98 -14.47 -36.64 -20.55 -29.50 -43.13 -37.98 37.02 86.68 19.47 29.75 14.96 69.80 19.35 23.21

Im) 25.87 16.11 7.63 28.59 33.10 20.30 144.47 156.71 125.63 122.12 127.40 94.40 104.43 138.80 64.48 61.49 -16.12 -8.92 -2.19 -1.80 -8.20 -2.24 -9.28 -22.06 -23.58 -27.22 B.94 32.07 20.34 -19.20 -23.41 17.25 16.77 -13.86 -27.65 47.33 52.45 -118.16 -55.73 3.10 B.21 -5.29 2.96 -98.50 -56.22 81.38 69.00 59.71 66.09 43.18 32.51 25.92 16.26 36.09 26.93 33.33 23.63 27.97 31.51 18.92 12.59 0.26 11.91 -3.77 -4.20 -11.37 0.93 -8.53 -6.06 37.19 39.78 41.94 43.58 47.15 43.25 43.83 42.51 40.96 41.83 39.16 12.10 12.04 41.07 36.20 34.99 40.03 45.32 18.34 22.44 26.25 22.55 22.15 20.03 111.39 113.61 112.73 117.44 97.92 100.83 107.13 98. 84 113.49 108.93 18.27 28.83 17.23 12.54 4.80 12.86 14.85 -4.94 14.57 -25.14 23.21 29.55 -11.39 -2.64 -3.79 -21.19 -23.24 -17.68 -29.94 -15.72 -38.05 -21.71 -31.48 -46.24 -40.00 34.02 85.08 17.69 27.87 12.95 67.91 13.86 21.19

Appendix 6.5 (confd)

DDH

R7693 R7801 R7802 R7804 R7805 R7806 R7809 R7810 R7811 R7312 R7814 R781S R7816 R7817 R7818 R7819 R7S20 R7826 R7844 R7872 R7873 R7874 R7875 R7876 R7922 R7924 R7925 R7926 R7927 R7928 R7929 R7930 R7931 R7932 R7933 R7934 R7935 R7936 R7937 R7938 R7939 R7940 R7941 R7942 R7943 R7944 R794S R791S R7947 R7948 R7949 R7959 R7961 R7973 R7977 R7978 R7979 R7982 R7991 R7992 R7993 R7994 R7997 R7998 R7999 R8002 R8004 R8012 R8044 R816S R8166 R8200 R8201 R8203 R8204 R8205 R8206 R8207 R8208 R8215 R8223 R8224 R8226 R8227 R8228 R8229

EASTING (ml

99986.92 98065.17 98000.22 98061.13 97971.82 98052.27 97109.51 97062.34 97050.13 97069.13 96927.91 96987.95 97000.22 97003.47 96684.88 97148.16 97381.31 97192.SO 97701.03 98187.00 98187.00 98136.92 98071.24 98140.05 98488.12 98546.15 97911.14 97910.53 97B73.11 97934.20 97942.21 97923.86 97906.46 97919.80 97931.92 97938.83 97856.40 97812.21 97797.50 97849.55 97879.22 97938.20 97972.45 97986.15 97987.03 98039.68 98113.34 98141.58 98193.36 98080.61 97971.24 98293.36 98356.06 97891.42 97817.21 97748.76 97685.97 98126.60 98067.07 97981.16 98133.57 98011.73 97632.07 98270.12 98194.86 95485.88 95266.86 95267.25 94532.68 93751.11 93487.69 97944.31 97814.51 98247.28 98292.32 98318.16 98318.05 98309.20 98383.49 98259.99 97527.53 97797.12 98127.74 98078.11 98092.16 98001.35

NORTHING ta)

194896.30 194496.41 194376.22 194373.41 194362.31 194442.47 195331.02 195339.77 195378.05 195444.56 195367.03 195436.11 194980.59 195000.36 195509.44 195400.05 196096.28 196290.02 196135.27 197250.00 197187.00 197249.05 197251.80 197185.02 196958.56 197001.92 194360.48 194389.94 194487.08 194389.09 194358.19 194422.73 194494.48 194366.70 194348.17 194332.91 194350.52 194321.66 194284.44 194379.05 194319.92 194540.23 194500.06 194412.08 194443.75 194387.80 194424.92 194421.55 194394.80 194400.20 194391.84 194527.36 194412.13 197176.08 197332.55 197328.63 197328.05 197063.94 197372.64 197411.83 197316.09 197176.80 197345.81 197432.31 197487.88 196767.91 197245.02 197505.67 196501.80 198648.56 198620.13 197622.84 197617.17 197120.44 197009.44 197180.94 197299.09 197360.56 197287.19 197306.45 196854.34 196872.33 197122.64 197124.67 197060.22 197117.70

COLLAR (m)

34.40 69.84 67.90 65.61 65.38 71.25 43.39 40.82 36.85 45.31 11.78 37.93 63.57 63.67 104.18 57.51 127.72 114.78 140.70 170.00 169.00 171.35 161.51 168.94 79.00 87.76 50.27 50.27 50.08 49.73 50.00 49.18 49.11 49.04 48.69 49.28 38.82 38.66 39.35 38.19 48.80 60.87 61.10 60.82 60.68 67.69 66.49 64.72 64.30 67.63 60.87 94.53 77.72 137.80 122.31 114.88 107.70 176.61 151.60 144.90 166.50 151.23 124.92 180.34 174.07 104.35 69.08 56.21 66.47 32.92 94.02 164.76 161.11 183.70 117.96 164.39 159.14 162.29 146.25 179.14 183.82 194.24 168.96 164.20 173.68 156.88

DEPTOP DEPBOT THICK TOPELEV BOTELEV

(») 15.88 60.04 53.33 65.66 52.50 51.36 37.42 31.60 28.36 37.61 23.80 27.05 18.70 21.26 77.58 56.60 164.14 164.26 136.54 176.70 173.22 172.31 170.40 171.08 17.15 127.03 32.30 30.61 41.77 30.27 34.60 33.81 38.84 32.50 36.60 45.18 21.72 23.85 40.20 20.87 37.50 51.40 45.42 42.28 39.80 52.14 52.62 55.35 80.56 51.00 42.90 79.55 41.31 174.46 165.30 173.27 175.34 167.43 159.77 171.40 166.41 164.42 170.76 176.20 183.02 188.56 178.88 166.61 15.77 126.42 37.20 211.11 211.75 166.77 122.20 137.00 143.88 151.52 110.00 180.35 228.38 220.60 161.19 162.60 174.62 156.99

Im) 48.00 72.18 60.68 78.32 59.35 57.26 46.52 39.57 34.71 40.54 32.99 33.94 19.82 24.46 86.00 65.95 169.62 173.12 137.14 183.34 178.98 181.82 178.04 177.60 17.50 133.59 38.55 36.40 51.43 35.68 40.54 39.74 49.00 38.38 43.17 51.80 27.62 29.75 52.48 26.61 44.43 59.89 51.76 48.44 45.70 58.32 58.49 62.20 90.50 57.70 48.72 86.48 45.01 174.90 171.51 179.71 183.05 173.46 166.48 176.50 167.48 173.27 178.07 183.28 190.63 190.52 181.04 169.03 16.66 126.75 87.75 217.20 220.26 172.42 127.97 144.00 151.22 158.18 113.90 187.35 237.28 225.68 178.72 169.40 179.44 167.10

Im) 2.12 10.91 7.35 12.66 6.85 5.90 9.10 7.97 6.35 2.93 9.19 6.89 1.12 2.82 8.42 9.35 5.48 8.26 0.60 6.64 5.76 9.51 7.64 6.52 0.35 6.56 6.25 5.79 9.66 5.41 5.94 5.93 9.08 5.88 6.57 6.62 5.90 5.90 12.28 5.74 6.93 8.49 6.34 6.16 5.90 6.18 5.87 6.85 9.62 6.70 5.82 6.29 3.70 0.44 5.19 6.11 7.71 6.03 6.58 5.10 0.71 7.65 7.31 7.08 7.61 1.96 2.16 2.12 0.89 0.33 0.55 6.09 5.09 5.65 5.77 7.00 7.31 6.66 3.90 7.00 8.90 5.08 3.91 6.80 2.36 1.33

Im) -11.18 9.80 14.57 -0.05 12.98 19.89 5.96 9.22 8.49 8.20 17.98 10.88 44.87 42.11 26.60 0.91 -36.42 -49.48 4.16 -6.70 -4.22 -0.96 -8.89 -2.14 61.85 -39.27 17.97 19.66 9.31 19.46 15.40 15.37 10.27 16.54 12.09 4.10 17.10 14.81 -0.85 17.32 11.30 9.47 15.68 18.54 20.88 15.55 13.87 9.37 -16.26 16.63 17.97 14.98 36.41 -36.66 -42.99 -58.39 -67.64 9.18 -8.17 -26.50 0.09 -13.19 -45.84 4.14 -8.95 -84.21 -109.8 -110.4 50.70 -43.50 6.82 -46.35 -50.61 16.93 25.76 27.39 15.26 10.77 36.25 -1.21 -41.56 -26.36 7.77 1.60 -0.94 -0.11

(ml -13.60 -2.34 7.22 -12.71 6.03 13.99 -3.14 1.25 2.14 5.27 8.79 3.99 43.75 39.21 18.18 -8.44 -41.90 -58.34 3.56 -13.34 -9.98 -10.47 -16.53 -8.66 61.50 -45.83 11.72 13.87 -1.35 14.05 9.46 9.44 0.11 10.66 5.52 -2.52 11.20 8.91 -13.13 11.58 4.37 0.98 9.34 12.38 14.98 9.37 9.00 2.52 -26.20 9.93 12.15 8.05 32.71 -37.10 -49.20 -64.83 -75.35 3.15 -14.88 -31.60 -0.98 -22.04 -53.15 -2.94 -16.56 -36.17 -111.96 -112.82 49.81 -43.83 6.27 -52.44 -59,12 11.28 19.99 20.39 7.92 4 .11 32.35 -8.21 -53.46 -31.44 -9.76 -5.20 -5.76 -10.22

Notes:

DEPTOP = Depth of top of Sangatta seam. DEPBOT = Depth of bottom of Sangatta seam. THICK = Thickness of Sangatta seam. TOPELEV= Elevation of top of Sangatta seam (above sea level). BOTELEV= Elevation of bottom of Sangatta seam (above sea level),

Appendix 6.6 Cored hole data for the Sangatta seam.

DDH

2044 2063 2089 2246 2264 2271 2282 2290 2320 2329 2331 2332 2334 2341 2343 2435 2442 2444 2517 2518 2519 2521 2522 2542 2552 2553 2554 2555 2556 2579 2585 2635 2638 2643 2644 2646 2670 2693 2694 2695 2696 2699 2711 2712 2713 2717 2724 2726 2760 2775 2810 2811 2812 2866 2867 2868 2869 2915 2916 2917 2918 2919 2920 2921 2922 2923 2924 2925 2926 2942 2944 2982 2983 2984 2985 2994 2995 2996 2999 3000 3001 3002 3003 3004 3005 3006 3007 3015 3016 3017 3018 3019 3020 3021 3022 3029 3030 3031 3032 3037 3038 3039 3040 3041 3042 3081 3141 3142 3143 3145 3147 3150 3151 3152

EASTING NORTHING

94929.20 197072.41 99429.40 201141.50 98776.40 197896.90 98788.70 195847.50 99086.46 198701.20 99910.38 204130.00 97370.20 195055.60 96712.31 194932.10 98873.24 195054.50 98904.90 200228.41 96330.61 19S022.40 96716.63 195565.30 98519.88 195243.70 97216.58 195589.30 98386.37 197435.90 95290.57 197746.45 97689.39 196985.40 96510.02 195505.69 98835.53 195505.30 98221.68 194515.30 97739.81 194243.50 97612.29 194761.20 97661.33 195438.40 94934.81 197759.59 96514.24 195987.30 96296.45 194759.30 96074.91 195750.90 96831.13 195233.50 97102.74 194754.30 96110.64 195500.70 98058.92 195009.40 98722.02 198250.00 94465.12 197752.20 97767.75 194501.40 98080.00 194755.30 98728.14 198581.70 98544.59 195956.80 99111.17 195404.20 99105.11 195294.30 98986.89 195356.00 98950.65 195841.70 97864.64 194738.10 99136.98 195506.89 98519.49 195498.53 98850.83 195856.91 96479.44 195006.06 97434.99 194740.31 98998.68 198805.84 99081.77 195305.61 96825.64 195511.98 99060.52 195293.40 99029.85 195272.60 99036.07 195328.00 99087.73 195317.10 99075.28 195311.50 99085.10 195305.40 99071.06 195299.10 98777.81 195251.10 98726.09 195366.90 98469.41 195373.90 98506.21 195625.20 98532.18 195766.10 98360.91 195741.60 98431.88 195881.00 98194.13 195519.40 98380.44 195128.30 98725.57 195124.60 98450.71 195001.60 99016.59 195505.40 101239.4 195215.77 101746.4 194996.20 96488.47 194598.30 96463.11 194871.40 96182.38 195126.00 96805.49 195046.10 99145.32 195339.10 98990.72 195434.40 99047.45 195453.80 97218.31 195262.00 96615.93 195246.00 96277.19 195457.40 96735.64 195382.30 96399.95 195752.10 96675.24 195742.30 96806.03 195761.20 96966.24 195487.10 96966.18 195359.60 97829.75 194311.30 98015.11 194496.70 98389.35 194517.10 98129.82 194619.30 97580.88 194497.90 97740.95 194775.70 97760.92 195014.00 98021.30 194867.60 97224.10 195326.30 99097.30 195322.60 97651.76 195194.00 97926.21 195242.90 97457.62 195272.80 97391.71 194879.50 97181.80 195127.00 97464.08 195498.20 97513.03 195746.91 97063.44 195746.10 98327.73 194757.00 98930.95 195250.00 99007.69 195088.00 98794.71 195004.80 98509.85 195120.00 98603.07 195130.40 98661.34 195258.60 98838.15 195377.20 98607.12 195378.90

ASH SULPHUR

0.00 0.99 1.30 0.90 1.40 1.31 2.45 1.32 2.26 1.10 1.68 5.70 1.95 4.25 1.50 0.00 1.70 2.50 1.80 2.31 1.50 2.91 3.25 0.00 2.90 0.80 2.80 2.32 2.30 1.78 4.40 1.10

o.oo 1.90 1.57 4.10 1.60 3.27 1.64 4.20 0.60

4.10 1.60 0.40 1.30 2.50 1.30 2.10 0.00 2.08 1.74 3.04 2.33 2.33 2.08 2.09 1.89 2.08 2.08 2.20 5.50 1.10 1.70 3.20 1.03 3.75 1.27 3.00 3.12 3.65 0.90 1.00 0.88 1.21 3.80 4.03 3.58 1.33 1.97 2.04 2.45 5.72 1.75 3.53 3.04 3.51 1.22 2.60 1.50 2.12 0.80 3.71 2.98 2.88 1.47 2.38 2.12 2.22 1.21 1.S7 1.47 1.47 2.64 0.88 0.92 1.35 0.98 1.70 3.08 1.47 2.51 3.82 4.00

0.00 0.22 0.87 0.21 0.24 0.62 0.17 0.49 0.57 0.28 0.78 0.30 0.24 0.15 0.20 O.OO 0.18 0.40 O.20 0.53 1.20 0.52 0.18 0.00 0.20 0.90 0.30 0.31 0.39 0.67 0.19 0.24 0.00 0.67 0.25 0.21 0.23 0.32 0.57 0.40 0.27

0.31 0.20 0.30 0.70 0.30 0.28 0.60 0.00 0.52 0.37 0.55 0.55 0.56 0.56 0.55 0.32 0.21 0.18 0.17 0.18 0.19 0.20 0.20 0.23 0.32 0.25 0.34 1.23 1.15 0.68 0.68 0.80 0.45 0.60 0.25 0.21 0.50 0.40 0.29 0.42 0.41 0.25 0.23 0.92 0.39 1.38 0.22 0.60 0.30 0.93 0.72 0.24 0.26 0.22 0.53 0.20 0.18 0.25 0.24 0.24 0.18 0.18 0.49 0.21 0.40 0.64 0.40 0.16 0.24 0.33 0.23 0.30

MOIS

5.00 5.20 6.30

5.10 6.20 4.93

6.29 5.40 4.49 5.59 5.00

4.90 5.90 5.10 4.71 4.60 5.01 4.80

6.60 6.38 6.60 5.29 5.01 4.98 4.51 5.30

4.52 4.61 5.80 4.70 4.93 5.12 4.70 4.80 4.92

4.50 5.00 6.40 5.60 5.70 5.00

4.96 4.91 4.92 5.19 5.10 5.15 5.04 4.66 5.16 5.27 5.70 5.60 4.80 4.60 5.00 5.92 5.02 5.01 4.60

6.44 6.09 6.07 5.41 6.60 4.77 4.98 6.39 5.97 6.62 6.02 6.30 5.73 6.04 5.57 5.80 5.14 4.93 4.80 4.46 5.25 5.11 4.54 4.60 4.75 5.26 4.85 5.09 4.79 5.06 5.62 5.04

5.66 4.76 4.67 4.67 4.50 5.12 4.60 4.62 4.67 4.60

VM

40.60 39.70 40.10

40.80 41.25 37.90

40.90 39.80 39.74 40.40 40.90

40.30 40.70 40.00 39.42 40.60 40.69 40.20

40.10 40.82 39.90 40.78 40.60 40.50 39.61 40.50

41.20 41.08 39.30 41.00 39.90 40.00 40.00 40.80 40.93

39.90 40.30 41.00 39.30 40.30 40.00

40.02 40.00 39.96 39.86 39.92 39.91 39.98 39.76 39.96 39.88 39.60 38.00 40.10 40.70 40.10 39.89 39.78 40.08 40.00

43.10 41.47 43.00 41.50 39.70 39.76 39.41 40.49 40.92 40.50 40.47 40.30 39.70 39.74 39.70 40.27 40.56 40.51 40.60 40.53 41.96 40.69 40.07 40.62 40.28 39.81 40.60 39.90 39.50 39.99 40.87 40.29

41.30 40.00 39.97 40.36 37.10 39.99 39.93 40.06 39.88 40.20

CV

13633.96 13610.51 13323.64

13682.74 13299.54 13057.13

13259.87 13547.54 13516.91 13334.35 13507.68

13334.35 13253.19 13363.08 13748.58 13784.90 13663.49 13505.00

13235.08 13206.07 13025.59 13416.95 13587.97 13190.39 13715.60 13502.43

13809.77 13849.37 13373.53 13620.49 13586.33 13352.05 14170.13 13935.90 13633.86

13183.31 13703.61 13318.06 13247.13 13448.93 13470.77

13548.91 13602.81 13770.05 13453.95 13506.07 13429.85 13493.90 13679.30 13528.22 13416.88 13325.57 13260.40 13601.50 13693.47 13983.24 13387.96 13550.86 13560.75 13486.17

13376.04 13266.50 13421.61 13507.45 13228.55 13667.35 13578.38 13365.33 13411.45 13428.37 13387.15 13299.69 13448.77 13374.51 13476.87 13411.05 13568.77 13740.25 13607.55 13643.49 13515.20 13526.76 13611.02 13771.23 13591.63 13422.02 13574.53 13535.53 13595.66 13537.41 13474.91 13555.83

13476.09 13584.36 13622.18 13751.96 13619.62 13542.18 13615.94

13607.06 13572.41 13743.18

THICK

3.50 6.33 5.04 6.57 7.20 6.61 7.92 8.69 5.59 5.18 6.49 7.49 7.37 4.60 8.07 1.50 6.18 8.15 8.91 4.86 8.09

10.53 4.26 1.10 8.20 6.40 4.70

11.36 6.34 5.06 5.06 6.46 1.00 3.66 7.67 5.44 7.13 4.48 5.90 9.10 6.95

4.08 2.99 5.08 7.28 9.36 5.01 6.05 9.47 6.88 7.73 8.41 7.99 7.67 7.75 7.32 10.05 7.44 5.60 8.85 9.51 5.60 7.14 6.99 5.55 4.36 5.92 6.35 3.57 3.75 7.99 6.73 6.64 9.53 9.20 9.69 6.70 6.71

10.48 6.30

12.50 9.10

13.40 6.05 4.17 9.71 5.75 7.32 5.34

10.22 7.44 11.11 3.22 7.38 9.94 B.75 6.93 2.64

11.59 7.33 6.01 7.01 4.34 5.33 6.38 4.79 5.99 5.99 6.77 6.70

6.27 8.00 2.40

1 DDH

3153 3154 3156 3157 3158 3159 3217 3219 3221 3222 3224 3225 3230 3231 3232 3233 3234 3236 3237 3368 3369 3388 3391 3392 3393 3395 3396 3397 3399 3400 3401 3406 3409 3410 3443 3445 3446 3454 3482 3484 3486 3491 3492 3493 3495 3496 3498 3500 3502 3507 3520 3521 3536 3537 3538 3539 3575 3576 3630 3631 3633 3634 3635 3637 3638 3639 3641 3694 3695 3696 3698 3699 3700 3701 3702 3703 3704 3705 3706 3721 3722 3724 3725 3729 3730 3731 3732 3733 7204 7232 7233 7264 7265 7280 7281 7282

Notes:

ASH

EASTING

98714.75 98371.54 98382.61 98364.93 98562.94 99020.05 98760.34 98909.44 98896.33 98822.34 98755.56 98814.59 98811.34 98758.27 98992.72 98906.30 98752.25 98823.58 98759.49 100025.3 100012.5 97515.52 99187.70 99215.15 99294.58 99265.07 99131.79 99168.54 98644.70 99505.51 97613.91 99018.30 99004.14 97617.33 99916.22 99260.97 98676.00 98763.63 96494.19 96632.53 96239.91 96364.22 96599.69 96834.88 96921.30 96848.11 96622.97 96882.57 96241.08 98732.33 99008.64 98349.19 97599.90 93344.20 98226.95 97655.50 99089.38 99110.00 97751.16 98019.06 97913.25 97914.93 97751.18 98228.17 98291.66 98248.27 97652.57 96961.65 96415.00 96716.89 96093.44 96216.27 96412.00 96410.00 96415.00 96265.00 96258.81 96812.00 96811.46 98893.62 98875.27 98843.17 98830.57 98746.15 98821.88 98835.85 98868.28 98858.42 96573.40 99130.58 99095.29 99067.90 99144.03 96045.00 96065.00 96080.00

= Ash

NORTHING

195503.20 195388.60 195505.00 195258.40 195024.00 195071.00 195447.98 195455.73 195575.09 195128.02 195066.52 195181.13 195181.60 195447.20 195612.60 195454.10 195065.90 195301.40 195066.80 203808.63 204475.77 195087.89 202491.70 202249.98 202020.34 201483.06 201020.63 200526.55 200254.97 203237.34 195127.88 195766.50 195767.40 195127.50 203758.02 203019.08 201463.09 199768.70 194680.20 194759.00 194822.60 195122.20 194882.10 194874.20 195032.20 195122.10 195082.38 194751.30 194904.20 195314.30 195098.01 195633.20 194610.20 194441.18 194619.80 194332.50 197195.60 198455.00 194904.04 194863.50 194628.62 194628.80 194901.70 194612.60 194476.40 194509.53 194325.80 195172.86 195320.00 195241.09 195441.14 195257.50 195300.00 195315.00 195320.00 195620.00 195626.00 195491.99 195490.80 195314.73 195308.50 195330.84 195316.76 195199.27 195228.81 195212.16 195139.17 195133.19 194584.88 195579.02 195595.18 195589.08 195557.42 195750.00 195695.00 195570.00

yield (adt

ASH SULPHUR

3.20 1.61 3.00 1.69 3.54 0.80 1.90 1.88 2.90 1.60 8.78 2.10 1.76 1.89 2.40 2.46 1.75 1.64 1.78 1.04 2.15 2.90 0.92 0.68 0.59 1.50 1.13 2.81 0.00 0.39 4.41 1.10 1.10 2.46 2.02 0.61 0.95 0.50 0.57 0.97 0.60 1.68 1.10 1.70 4.15 1.80 1.50 3.90 0.98 2.23 1.06 2.78 2.74 0.00 5.60 2.13 0.00 1.00 0.00 1.23 0.00 0.00 2.20 0.00 O.OO 0.00 0.00 0.00 0.00 0.00

o.oo 2.25 0.00 0.00 2.52 0.00 2.63 0.00 1.60 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

o.oo 0.00 0.00 0.00 0.00

, %) !

0.24 0.18 0.61 0.19 0.43 0.70 0.30 0.19 0.50 0.30 0.46 0.40 0.33 0.25 0.36 0.21 0.33 0.37 0.34 0.48 1.05 0.20 0.77 0.91 0.94 0.80 0.44 0.24 0.00 0.18 0.17 0.26 0.26 0.19 1.46 0.57 0.32 0.19 0.65 0.57 0.70 0.66 0.53 0.41 0.34 0.31 0.50 0.43 0.97 0.28 0.29 0.20 0.69 0.00 0.26 1.10 0.00 0.20 0.00 0.30 0.00 0.00 0.17 0.00 0.00 0.00 0.00 0.00 0.00 0.00

o.oo 0.51 0.00 0.00 0.62 O.OO 0.97 0.00 0.21 O.OO 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00 0.00

o.oo

MOIS

5.20 5.10 4.80 5.21 4.53 4.60 4.60

5.30 4.00

6.70 4.96 4.67 4.70 4.53 4.71 4.10 4.68

4.70

4.30 4.30 5.04

5.70 5.19 5.03 5.50 6.20 6.05 5.63 5.51 5.70 6.00 5.80 6.45 4.89

5.41 4.92

4.80 5.09

5.80

4.83

5.00

7.10

5.75

5.42

4.95

VM

40.10 39.98 39.80 39.92 40.06 40.60 40.40

40.00 40.00

40.10 39.90 40.37 40.40 40.01 38.90 40.13 39.00

40.90

41.20 41.20 40.12

42.00 42.68 41.97 42.20 41.86 41.69 41.90 40.64 41.90 41.10 40.25 41.52 40.41

39.61 41.57

40.40 41.12

41.10

41.84

41.30

41.65

41.10

41.98

41.30

rom composite core SULPHUR = Sulphur content (adb, %) 1 MOIS VM cv THICK

= Moisture content (adb, %)

CV

13765.92 13549.21 13690.81 13524.69 13604.19 13806.64 13639.50

13640.95 13701.16

13840.55 13613.98 13675.65 13607.86 13526.08 13610.64 13716.36 13600.69

13772.71

13730.96 13730.96 13597.77

13454.82 13321.73 13310.67 13176.31 13290.18 13299.46 13421.38 13399.42 13408.01 13340.81 13403.35 13158.77 13630.22

13509.06 13714.59

13797.61 13674.91

13379.21

13610.86

13611.64

13304.11

13283.62

13341.84

13396.26

samples.

THICK

4.24 7.22 7.90 . 3.24 5.70 9.32 6.79 7.41 6.08 4.82 5.19 2.45 3.34 6.56 7.42 7.64 5.26 B.39 5.19 4.87 3.71 5.77 6.67 6.43 6.45 7.59 6.34 8.31 9.75 6.34 3.88 0.46 4.68 5.20 5.27 6.18 2.93 5.82 6.19 7.08 6.32 6.89 7.15 8.06 9.41

11.11 B.72 5.83 6.30 7.05 5.96

10.02 7.71 6.04 7.68 4.00 6.51 6.64 7.00 7.31 9.00 8.85 7.00 8.00 5.83 7.16 5.35 7.09 7.13 12.38 5.18 6.77 6.70 7.17 7.17 8.19 8.22 10.40 11.46 9.04 2.00 5.79 6.23 0.50

10.02 9.57 5.52 5.78 4.50 2.85 2.03 1.32 2.12

10.95 11.09 10.53

rom composite core samples. from composite core samples.

= Volatile matter content (adb, % = Cal Drific values (mmmr, cal/g) = Thickness.

from composite lore 3am from composite core sampl

Appendix 6.7 Ply samples data for the Sangatta seam.

DDH EASTING NORTHING SAMP. No. DEPTOP DEPBOT

C2063 99429.40 C2063 99439.40 C2063 99439.40 C2063 99429.40 C2063 99439.40 C2063 99439.40

301141.50 SN 201141.50 SN 301141.50 SN 301141.50 SN 201141.50 SN 201141.50 SN

10011 10012 10013 10014 10015 10016

C2099 98776.40 197896.91 SNCM10031 C2089 98776.40 197896.91 SNCM10033 C2089 98776.40 197896.91 SNCM10033

C2194 104845.60 C2194 104845.60 C2194 104845.60 C2194 104845.60 C2194 104845.60

205537.59 SN 305527.59 SN 205527.59 SN 305537.59 SN 20S537.59 SN

10093 10094 10095 10096 10097

C2346 C2246 C2246 C2246 C3346 C2246 C3346 C3246

98788.70 98798.70 98788.70 98788.70 987 98.70 98788.70 99788.70 98788.70

C2264 99086.46 C2264 99086.46 C2264 99086.46 C2264 99086.46 C2264 99086.46 C2264 99096.46 C2264 99086.46

C2271 C2271 C2271 C2371 C2271 C2271 C2271 C2371

C2282 C2383 C32S2 C3282 C2283 C2282 C2282 C2282 C2282 C2282

C3290 C3290 C2290 C2390 C2290 C2290 C2290 C2290 C2390

C3320 C2320 C2330 C2320 C2320 C3320 C2320 C2330 C2320

C2329 C2329 C2329 C2329 02329 C2329 C3339

C2332 C2332 C3332 C2332 02332 C2333 C2332 C2333 C2332 C2332 C2332 C2332 C2333

C2341 C2341 C2341 C2341 C2341 C2341 C2341 C3341 C3341 C2341

C2343 C2343 C2343 C2343 C2343 C2343 C2343 C2343

99910.39 99910.39 99910.38 99910.39 99910.38 99910.38 99910.38 99910.39

97370.20 97370.20 97370.20 97370.30 97370.30 97370.20 97370.20 97370.30 97370.30 97370.20

96712.31 96712.31 96712.31 96712.31 96712.31 96713.31 96713.31 96713.31 96713.31

98973.24 99973.24 98873.21 98873.24 99873.24 98873.24 98973.24 99873.34 98873.24

99904.90 99904.90 98904.90 98904.90 98904.90 98904.90 98904.90

96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63 96716.63

97316.58 97316.58 97316.58 97216.58 97316.58 97316.58 97316.59 97316.59 97316.58 97216.58

98388.37 99388.37 99388.37 98388.37 98388.37 98388.37 98388.37 98398.37

C2518 C3S19 C2S18 C2518 C2518 C2518 C2518

C2519 C2519 C2519 C2519 C2519 C2519 C2519 C2519 C2619 C2519 C2519 C3S19 C2519

98221.68 98321.68 98321.69 99231.69 98331.69 98331.68 98221.68

97739.81 97739.81 97739.81 97739.81 97739.81 97739.81 97739.81 97739.81 97739.81 97739.81 97739.91 97739.91 97739.81

195917. 195847. 195947. 195947. 195847. 195847. 195847. 195847.

198701. 198701. 199701. 198701. 198701. 198701. 198701.

204130. 304130. 204130. 304130. 304130. 304130. 204130. 204130

195055 195055 195055 195055 195055 195055 195055 195055 195055 195055

50 SNDT10144 50 SNDT10145 50 SNCH10146 50 SNCM10147 50 SNCM10148 50 SNCM10149 50 SND810150 50 SNDBDO150

20 SNDT10170 20 SNCM10171 20 SNCM10172 20 SNCH10173 20 SNCM10174 20 SNCM10175 20 SNDB10176

00 SN 00 SN 00 SN 00 SN 00 SN 00 SN 00 SN 00 SN

10177 10178 10179 10180 10181 10182 10183 10184

59 SNOT10209 59 SNCM10209 59 SNCM10210 .59 SNCM10311 .59 SNCH10312 .59 SNCM10213 .59 SNCM10214 .59 SNDB10315 .59 SNDB10216 .59 SNDB10217

C3443 97689.39 C3442 97689.39 C3413 97699.39 C3443 97689.39 C2443 97699.39 C2442 97689.39 C2442 97699.39 C2442 97689.39

C2517 99835.53 C2517 98835.53 C2517 98835.53 C2517 98935.53

194932.09 194932.09 194933.09 194933.09 194932.09 194933.09 194933.09 194932.09 194932.09

195054.50 195054.50 195054.50 195054.50 195054.50 195054.50 195054.50 195054.50 195054.50

200333.41 300328.41 300328.41 200229.41 200228.41 200228.41 200338.41

195565.30 195565.30 195565.30 195565.30 195565.30 195565.30 195565.30 195565.30 195565.30 19S565.30 195565.30 195565.30 195565.30

195589.27 195589.27 195589.27 195589.27 195589.27 195589.27 195599.27 196589.27 195589.37 195589.27

197 435.88 197435.88 197435.88 197435.88 197435.98 197435.88 197435.89 197435.88

196995.43 196985.43 196985.42 196985.42 19699S.42 196985.42 196985.42 196985.42

195505.30 195505.30 195505.30 195505.30

194515.27 194515.27 194515.37 194515.27 194515.27 194515.37 194S15.27

194343.47 194343.47 194343.47 194343.47 194343.47 194343.47 194343.47 194343.47 194243.47 194243.47 194343.47 194343.47 194243.47

SNDT10264 SNCM10265 SNCH10366 SNCM10267 SNCH10268 SNCM10269 SNCM10270 SNDB10371 SNDB10372

SNDT10279 SNCM10380 SNCM10381 SNCH10283 SNCM10283 SNCM10284 SNDB1028S SNDB10386 SNDB10287

SN 10313 SN 10314 SN 10315 SN 10316 SN 10317 SN 10318 SN 10319

SNDT10343 SNCM10344 SNCM1034S SNCM10346 SNCM10347 SNCM10348 SNCM10349 SNCM10350 5NDB10351 SNDB10352 SNDB10353 SNDB10354 SNDB103S5

SHDT10451 SNDT10452 SNDT10453 SNDT104S4 SNDT10455 SNCH104S6 SNDB10457 SNDB10469 SNDB10459 SNDB10460

SNOT10495 SNCH10496 SNCM10497 SNCH10499 SNCM10499 SNCM10500 SNCM10S01 SNDB10502

SNDT10948 SNCM10849 SNCM108S0 SNCM108S1 SNCM109S2 SNCH10853 SNCM10854 SNDB10855

SNDT10603 SNDT10604 SNCM1060S SN 10616

SNDT10633 SNCM10634 SNCM1063S SNCH10636 SNCH10637 SMDB10638 SNDBD0638

SNDT10640 SNCH10641 SNCM10642 SNCM10643 SNCH10644 SNCM1064S SNCM106 46 SNCM106 47 SNCM10648 SNCM10649 SNDB10650 SNDB10676 SNDB10677

30.730 31.480 32.530 33.480 34.940 36.140

46.210 48.050 49.620

77.060 78.050 79.450 80.600 82.140

33.970 33.590 33.830 35.630 36.310 38.280 40.160 40.160

51.420 51.520 53.800 54.220 55.780 57.250 58.730

66.960 67.060 68.510 69.920 70.700 71.540 73.400 73.410

132.280 132.380 123.640 135.180 136.450 127.900 128.780 129.950 130.050 130.300

80.500 80.610 81.590 83.800 84.380 84.790 86.630 88.270 89.300

32.390 33.490 33.260 33.900 35.300 36.960 37.460 37.580 38.080

71.760 71.860 73.000 74.120 75.760 76.110 76.840

93.530 93.650 93.690 94.800 95.650 96.640 96.910 97.630 98.530 98.640 99.710 99.830

100.140

106.390 106.490 107.030 107.170 107.570 107.880 109.610 109.960 110.650 111.090

31.490 32.530 33.480 34.940 36.140 37.060

48.050 49.630 51.250

78.050 79.450 80.600 83.140 83.370

33.590 33.830 35.630 36.810 38.380 10.160 10.760 10.360

51.530 52.800 54.220 55.780 57.250 58.720 58.830

67.060 68.510 69.930 70.700 71.540 73.400 73.410 73.570

122.390 123.640 125.180 126.450 137.900 138.780 139.950 130.050 130.300 130.400

80.610 81.590 83.800 84.280 84.790 86.620 88.270 89.300 89.400

33.490 33.260 33.900 35.300 36.860 37.460 37.580 38.080 38.180

71.860 73.000 74.130 75.760 76.110 76.840 76.940

93.650 93.690 94.800 95.650 96.640 96.810 97.620 98.530 98.640 99.710 99.830

100.140 100.240

106.490 107.030 107.170 107.570 107.880 109.610 109.960 110.650 111.090 111.190

RD

1.33 1.33 1.31 1.33 1.33 1.33

ASH HOIS VM

1.58 8.16

108.000 108.740 110.100 111.290 113.290 113.600 113.600

110.530 110.650 110.760 111.750 113.020 114.210 115.800 116.480 117.610 118.210 118.400 118.560 118.850

.90

.75

8.73 7.59 7.61 7.91 7.96

1.33 3.43 5.35 1.30 .53 5.40 1.39 .96 4.83

1.85 43.30 8.90 1.39 1.40 14.00 1.39 1.80 13.80 1.36 1.10 13.50 3.63 88.60 3.00

2.63 89.80 1.57 JO.80 1.30 1.00 1.30 .40 1.39 .10 1.39 1.40 2.54 84.40 3.54 94.40

1.91 55.50 1.32 1.31 1.30 1.39 1.32

3.10 1.30 5.40 5.00 5.10 1.80 2.70 2.70

4.70 6.40 6.70 6.70 6.20 6.10 3.60

3.73 8S.10 3.50 2.30

.20

.20 4.10

1.50 .90

1.33 1.34 1.32

3.54 84.10 1.31 3.50 1.30 1.32 1.30 1.33

.60 3.8

1.31 5.80 2.67 86.30 1.45 17.70 3.53 85.90

3.53 79.10 1.40

1.30 1.30 1.34 1.31 1.32 1.31 3.S4 86

.60 1.10

.50

.90

8.40 . 8.60 . 7.90 8.10 8.60 8.80 . 8.30

3.40 5.70 5.30 5.70 5.80 5.30 4.70 2.40 4.50 3.10

2.80 4.90 6.30 6.40 6.20 6.30 6.20 S.30 2.SO

2.65 84.70 3.40 1.34 1.33 1.31

6.30 5.60 .70

4.SO

1.32 1.30 1.40 2.55 87.80 1.32 4.60 2.54 84.60 3.10

5.30 5.10 4.40 3.70 4.SO

141.300 141.400 141.400 143.700 143.700 144.200 144.300 145.630 14S.630 146.640 146.640 147.810 147.810 149.470 149.470 149.570

200.460 300.960 300.860 302.540 303.540 303.350 303.350 205.000 205.000 205.630 305.630 307.090 207.090 207.640 307.640 207.750

34.970 35.090 35.090 35.370 35.370 36.430 44.000 44.070

2.33 76.10 1.33 1.10 1.33 .60 1.33 .90 1.87 49.50 1.34 4.40 3.60 88.50

2.05 61.30 1.31 .80 1.33 3.30 1.31 1.90 1.31 3.20 1.56 15.60 1.31 1.00 1.34 4.30 3.61 78.60 1.36 4.80 1.77 44.00 1.36 5.50 3.60 86.40

2.62 90.30 1.40 9.80 2.03 61.30 1.36 5.70 2.OS 64.90 1.33 4.60 1.73 44.60 1.64 35.10 1.46 19.30 1.77 47.20

3.02 63.80 1.32 4.30

4.30 7.40 7.30

6.20 2.70

4.10 S.60 5.70 S.60 5.60 4.80 5.60 S.50 2.20 5.60 1.30 S.60 2.50

.30

.30 1.30 1.31

1.60 .70

1.60 1.39 1.10 2.30 75.20

1.89 56.10 1.29 1.80 1.28 .SO 1.29 1.10 1.30 1.30 1.30

1.00 1.90 3.10

4.90 S.20 4.10

S.70 S.30 S.30 4.90 S.20 3.00

4.30 5.30 S.30 5.00 4.90 4.70 1.70

1.73 43.30 3.8

3.33 71.30 1.40 15.10 1.33 S.10 3.24 74.40 3

3.8

108.740 110.100 111.390 113.390 113.600 113.790 113.700

130.650 110.760 111.7S0 113.030 114.210 115.800 116.480 117.610 118.210 118.400 118.560 118.850 119.010

2.46 78.00 1.33 3.10 1.30 1.40 1.34 3.90 1.31 1.10 1.76 44.60 1.76 44.60

3.44 71.70 1.67 34.30 1.34 6.20 1.39 1.29 1.29 1.35 1.30 1.30

.30

.90

.30 6.40 1.00 1.10

1.41 11.80 2.11 6S.20 1.43 16.80 2.04 63.70

3.30 4.70 4.40 4.30 4.70 4.00 1.00

2.50 3.00 3.SO 4.30 4.70 4.80 4.10 4.60 4.40 3.70 3.80 3.30 2.90

.29

.16

.28

.51

.17

.23

.30

.26

.26 1.70 1.70

.43 .38 .34

.19

1.14 1.55 .45 .46 .36 .27 .25 .35

.07 .27

.14

.17

.01

4.94 2.16 .71 .26 .18 .17 .20 .22 .38

.65

.67

.43

.38

.17

.29

.36

.46 1.87 .51 .28

.17

.16

.13

.14

.17

.17

.16

.22

.19

.19

.17

.13

.13

.17

.15

.14

.IS

.14

.35 1.51

.21 .21 .16 .14

1.89

.31 1.01 .30 .21

3.67

.42

8.57 4.83 2.62 1.46 .71 .55 .65 .84

1.14 1.3S .77

4.36 1.91

DDH EASTINO NORTHINO SAMP. No. DEPTOP DEPBOT ASH HOIS VM CV SULPHUR

C2519 97739.81 194243.47 SNDBD0677 118.8S0 118.950 2.04 63.70 3.90 -

C2521 C2S31 C3531 C3531 C2531 C3531 C3531 C3531 C2S21 C3531 C3S31

97613.39 97612.39 97613.39 97613.29 97613.39 97613.39 97612.39 97613.39 97613.29 97613.29 97613.39

C2523 97661.33 C2522 97661.33 C2523 97661.33 C3S33 97661.33 C2523 97661.33 C3S22 97661.33

C2552 C2552 C25S3 C25S2 C2S52 C25S2 C3553 C2S52

96514.24 96514.34 96514.34 96S14.24 96S14.34 96514.34 96514.34 96514.31

C3553 96396.15 C3553 96296.45 C2553 96296.45 C2553 96396.45 C2553 96396.45 C3S53 96396.15 C25S3 96396.45

C3554 96074.91 C3554 96074.91 C2554 96074.91 C3S54 96074.91 C2554 96074.91 C25S4 96074.91

C3555 C2555 C2555 C3SSS C2555 C2555 C2555 C255S C255S C35S5 C2SS5 C2555 C2S55

C2SS6 C2S56 C2556 C25S6 C25S6 C2SS6 C2SS6

C2S79 C2S79 C3S79 C2579 C2579

C2S8S C3S85 C258S C2585 02585 C258S C3S85 C2585 C2585 C2S85

C2635 C2635 C2635 C2635 C2635 C2635 C2635

C2643 C2643 C2643 C2643 C2643 C3643 C3643 C2643 C2643 C2643

C3644 C2644 C2644 C2644 C2644 C2644 C2644 C3644 C2644

C2646 C2646 C3646 C3646 C2646 C2646 C2646 C2646 C2646 C2646 C3646 C2646

C2670 C3670 C3670 C2670 C2670 C2670 C2670 C2670 C2670 C2670 C3670 C3670

C3693 C2693 C2693 C2693 C2693 C2693 C2693 C3693 C3693 C3693

194761 154761 194761 194761 194761 194761 194761 194761 194761 194761 194761

20 SNDT10688 20 SNDT10689 30 SNCM10690 30 SNCM10691 30 SNCM10693 30 SNCH10693 30 SNCH10694 20 SNCH10695 20 SNCM10696 20 SNCM10697 20 SNDB10698

99.050 98.150 99.770 99.890

101.050 102.310 103.610 104.790 106.300 107.440 108.680

98.150 99.770 99.890

101.050 103.310 103.610 104.790 106.300 107.440 108.680 108.800

195438.36 SNDT10714 US.210 135.340 195438.36 SNCH10715 135.340 136.390 195438.36 SNCM10716 136.390 137.940 195439.36 SNCM10717 137.840 139.110 195438.36 SNCH10718 139.110 139.600 195438.36 SNDB10719 139.600 139.700

195987. 195987. 195987. 195987. 195987. 195987. 195987. 195987.

34 SNDT10749 154. 34 SNCH107 50 355. 34 SNCH10753 157. 34 SNCM10753 158. 34 SNCM10753 169. 34 SNCM107S4 160. 34 SNDB10755 161 34 SNDB10756 163.

270 155.590 590 157.000 000 158.100 100 159.060 060 160.910 810 161.440 140 162.370 370 163.470

194759.31 SNDT10760 194759.31 SNCM10761 194759.31 SHCM10762 194759.31 SNCM10763 194759.31 SNCM10764 194759.31 SNCM10765 194759.31 SNDB10766

195750.89 SNDT10773 195750.99 SNCH10774 195750.89 SNCH10775 19S750.99 SNCM10776 195750.B9 SNDB10777 195750.89 SNDB10778

96831.13 96831.13 96931.13 96831.13 96931.13 96831.13 96831.13 96831.13 96831.13 96831.13 96831.13 96831.13 96831.13

97102.74 97102.74 97102.74 97103.74 97103.74 97103.74 97103.74

96110.64 96110.64 96110.64 96110.64 96110.64

98058.92 98058.92 99058.93 98058.92 98058.92 98058.92 98059.93 98058.92 98058.92 98058.92

98722.02 997 33.02 98723.03 98732.02 98722.02 98722.03 98723.02

977 67.75 97767.75 97767.75 97767.75 97767.7S 977 67.75 977 67.75 977 67.75 977 67.75 97767.75

98080.00 98080.00 99080.00 98080.00 99080.00 98080.00 98080.00 98090.00 98080.00

99738.14 99728.14 98728.14 99728.14 98728.14 98728.14 98728.14 99728.14 99728.14 99728.14 98728.14 98728.14

98544.59 98544.59 98544.59 98544.59 98S44.S9 98S44.59 99544.59 99544.59 985 44.59 99544.59 98544.59 98544.59

99111.17 99111.17 99111.17 99111.17 99111.17 99111.17 99111.17 99111.17 99111.17 99111.17

195333.52 195233.52 195233.52 195233.53 195233.52 195233.53 195233.52 195233.52 195233.52 195233.52 195233.52 195233.52 195233.52

194754.34 194754.34 194754.34 194754.34 194754.34 194754.34 194754.34

195500.66 195500.66 195500.66 195500.66 195500.66

SNDT10779 SNCM107 80 SNCM10781 SNCM107 83 SNCM10783 SNCH10784 SNCM10785 SNCM10786 SNCM10787 SNCM107 88 SNDB10789 SNDB107 90 SNDB107 91

SNDT107 92 SNCM10793 SNCM107 94 SNCH10795 SNCM10796 SNCH10797 SNDB107 99

SN 10918 SNCH10819 SNCH10820 SNDB10821 SNDB10833

195009 195009 195009 195009 195009 195009 195009 195009 195009 195009

44 SNOT10655 .44 SNCM10656 .44 SNCM10657 .44 SNCM10658 44 SNCM10659 44 SNCM10660 .44 SNCM10661 .44 SNDB10662 .44 SNDB10663 .44 SNDB10664

43.170 43.270 44.380 46.200 47.650 48.800 49.670

29.450 29.550 30.650 31.900 33.000 34.350

37.830 37.970 38.970 40.560 11.620 13.570 13.120 14.510 46.040 47.210 18.490 18.940 49.330

36.320 36.430 37.500 38.490 40.090 41.570 42.760

35.200 36.090 38.060 39.670 40.260

62.130 62.590 63.090 63.160 64.480 65.500 66.170 67.460 67.640 68.380

43.370 44.380 16.200 17.650 18.800 19.670 19.770

29.550 30.650 31.900 33.000 31.250 34.380

37.970 38.970 10.560 11.620 12.570 13.420 14.510 46.040 47.210 48.490 49.940 19.330 49.440

36.420 37.500 38,490 40.090 11.570 12.760 42.860

36.090 38.060 39.670 40.260 40.410

62.590 63.090 63.160 64.480 65.500 66.170 67.460 67.640 68.280 68.380

194501. 194501. 194501. 194501. 194501. 194501. 194501. 194501. 194501. 194501.

38 SNDT109 86 38 SNCM10987 38 SNCM10988 38 SNCM10989 38 SHCH10990 38 SNCM10991 39 SNCM10992 38 SNCH10993 38 SNDB10994 38 SNDB1099S

194755.35 194755.35 194755.25 194755.25 194755.25 194755.25 19475S.3S 194755.35 194755.25

SNDT11005 SNCM11006 SBCK11007 SNCM11008 SNCM11009 SNCH11010 SNCH11011 SNDB11012 SNDBD1012

198591 198581 198581 198581 199581 198581 198581 198581 199581 198581 198581 199581

69 SNDT11045 69 SNCH11046 69 SNCH11017 69 SNCM11048 69 SNCH11049 .69 SNCM110SO 69 SNCH11051 .69 SNCH11052 69 SNCM11053 69 SNCM11054 .69 SNCH110S5 69 SND811056

195956.77 19S9S6.77 195956.77 195956.77 195956.77 195956.77 195956.77 195956.77 195956.77 195956.77 195956.77 195956.77

195404.17 195404.17 195404.17 195404.17 195404.17 195404.17 195404.17 19540 4.17 195104.17 195404.17

SNDT11068 SNCM11069 SNCH11070 SNCM11071 SNCM11073 SNCM1107 3 SNCM11074 SNDB1107S SNDB11076 SNDB11077 SN 11079 SN 11079

SNDT11090 SNCH11081 SNCH11082 SNCMI1083 SNCM11084 SNCH11085 SNCM11086 SNCH11087 SNCH11088 SNDB11089

135.180 125.280 126.750 127.800 129.210 130.290 131.610 132.750 133.830 133.940

103.550 102.650 104.010 105.310 106.520 107.630 108.940 110.320 110.320

79.680 79.780 80.240 81.460 81.570 B2.480 82.820 83.730 83.820 84.380 84.650 85.230

36.170 26.270 27.270 28.270 29.240 30.350 31.350 33.420 32.S40 12.860 33.400 33.850

13.530 13.640 14.160 14.660 15.200 15.7 00 16.140 17.000 17.400 18.120

1.68 37.40 1.34 6.10 2.03 60.20

.90 5.00 -

1.30 1.29 1.34

.70 6.70 .40 .30

1.00 7.

4.40 5.00 5.30 4.70 4.10

2.55 87.20 2.10

2.35 76.60 1.33 6.10 1.32 3.90 1.33 1.50 1.34 3.60 3.36 78.70 2.20

4.50 4.90 4.70

1.30 1.50 1.30 1.20 1.29 .70 1.40 11.60 1.30 1.20 1.29 1.10 1.30 3.00 1.62 35.90

1.77 41.00 31 .40

.40

.40

198249.95 SNCM10956 103.540 104.700 198249.95 SNCH10957 104.700 105.830 198249.95 SHCH10958 105.830 106.920 196249.95 SNCH10959 106.920 108.170 198249.95 SNCH10960 108.170 109.070 199249.95 SNCM10961 109.070 110.000 198249.95 SNDB10962 110.000 110.100

1.30 1.31 1.33 1.31 .70 2.24 69.90

1.98 51.60 1.35 6.00 1.33 1.20 1.32 .50 1.33 1.20 2.30 75.70

1.65 38.40 1.31 1.60 1.30 1.00 1.42 11.90 1.31 1.30 1.30 1.32 1.31 1.31 1.30

49.30 1.70

6.00 5.80 6.40 S.90 6.20 5.90 S.50 4.90

4.30 5.60 6.30 6.60 6.60 6.10 5.00

4.50 6.40 7.10 6.50 7.10

3.90 S.30 5.30 4.90 5.50 5.70 S.40 5.00 5.80 5.40

1.91 56.40 3.00 -

2.2S 71.00 1.35 6.00 1.32 1.30

4.50 1.20 .70

1.00

2.90 5.00 5.00 5.40 5.SO 4.70

2.35 78.20 2.90

1.29 1.00 6.60 1.32 1.90 6.80 1.31 .70 7.20 1.31 1.90 6.SO 1.96 56.80 4.50

2.33 77.70 1.33 6.20 2.32 77.90 1.28 1.80 1.29 .40 1.30 1.50 1.28 .09 1.56 31.10 1.29 3.60 2.47 83.70

3.90 4.90 4.00 4.80 4.90 5.00 4.50 3.10 4.20 3.30

1.34 2.30 S.20 -1.32 .50 5.60 -

.50

.30

125.280 126.750 127.800 129.240 130.250 131.610 132.750 133.930 133.940 134.040

102.6S0 104.010 105.210 106.520 107.630 108.940 110.320 110.420 110.420

79.780 80.240 81.460 81.570 82.480 82.320 83.730 83.820 84.380 84.650 85.220 8S.320

26.270 27.270 28.270 29.240 30.350 31.350 33.420 32.540 32.860 33.400 33.500 34.240

13.640 14.160 14.660 15.200 15.700 16.140 17.000 17.400 18.120 18.220

1.32 1.31 1.29 1.32 3.40 2.56 90.60

2.27 69.50 1.29 2.10 1.29 1.00 1.29 1.32 1.29 1.29 1.29 1.58 32.70 2.13 69.30

1.10 3.80 .50 .20

4.90 2.10

2.20 3.90 4.80 4.70 4.20 4.50 4.70 3.60 3.60 2.90

2.51 83.00 2.40 1.30 1.30 4.40

2.40 .60 .60 .40

1.29 1.29 1.29 1.29 1.29 2.46 94.10 2.46 84.10

2.24 74.50 1.36 10.00 1.30 1.20 1.80 45.30 1.32 2.30 1.63 35.60 1.31 .60 1.77 46.40 1.30 1.60 1.35 S.30 1.33 1.70 2.02 62.90

2.23 73.90 1.34 6.90 1.30 .90 1.30 .40 1.29 .40 1.

4.40 4.SO

3.20 1.60 5.30 3.80 5.50 1.00 5.50 3.SO

90

3.00 6.90 4.30 .90 4.60 .40 4.70 .40 4.70 .50 4.60

2.00 4.20 2.29 79.20 1.29 2.00 1.75 46.30 2.59 88.70 1.30 2.20

2.50 81.70 1.37 9.30

3.50 2.90 2.00

1.30 1.30 1.30

.60

.70 7.30 1.35

1.28 .80 1.48 24.30 2.34 81.10

4.70 4.60 4.20 3.80 3.20 2.20

1.91

4.32 2.78 1.57 1.73 .73 .32 .22 .17 .20 .25 .37

.20 .26 .15 .14 .16 .14

.15

.17

.19

.18

.17

.21

.24

2.28 1.02 .50 .36 .36

1.10

1.S1 .34 .22 .19 .22 .19

1.31 1.14 .27

.16

.15

.16

3.08 1.35 .35

.19

.20

.21

.31

1.23 .35

.17

.16

.14

.15

.16

.16

.30

.20

6.16 2.01

.22

.20

2.32 .48 .23 .16 .17 .23 .23 .28 .28

.31

.17

.19

.22

.32

.22

.61

.29

.23

.30

.21

.18

.20

.17

.33

.15

.19

.25

.21

.IS

.15

.16

.14

.18

.21

C2694 99105.11 195294.34 SNDT11090 7.640 7.780 2.S2 86.40 3.00 -

Appendix 6.7 (cont'd)

DDH EASTINO NORTHINO SAMP. No. DEPTOP DEPBOT

C2694 99105.11 C2694 99105.11 C2694 99105.11 C2694 99105.11 C2694 99105.11 C3694 99105.11 C3694 99105.11 C3694 99105.11 C2694 99105.11 C2694 99105.11 C2694 99105.11 C2694 99105.11 C2694 99105.11

C2695 98986.99 C3695 99996.99 C3695 98986.89 C3695 98986.89 C3695 98986.89 C2695 98986.89 C2695 99996.89 C2695 98986.89 C3695 98986.89 03695 98996.89 C3695 98986.89 C3695 98996.89 C3695 98986.89 C2695 98986.89 C2695 99996.89 C2695 98986.89 C2695 98996.89 C3695 98986.89 C2695 98986.89

C2696 98950.65 C2696 98950.65 C2696 98950.65 C2696 98950.65 02696 98950.65 C2696 98950.65 C2696 98950.65 03696 98950.65 C2696 98950.65 C2696 98950.65

C2754 101690.79 C3754 101680.79 C2754 101680.79 C3754 101680.79 C2754 101680.79 C2754 101680.79

C2810 99060.52 C2910 99060.53 C2810 99060.52 C2810 99060.52 C2910 99060.52 C2810 99060.52 C2810 99060.52 C3810 99060.52 C2810 99060.52 C2810 99060.52 C3810 99060.53

C2811 99029.85 C2811 99029.85 C2811 99029.85 C2811 99029.95 C2811 99039.85 C2811 99029.95 C2811 99039.85 C2811 99029.95 C2811 99039.95 C3811 99039.85 C3811 99039.85

C3813 99036.07 C3813 99036.07 C3813 99036.07 C2812 99036.07 C2812 99036.07 C2813 99036.07 C3813 99036.07 C3813 99036.07 C2812 99036.07 C2912 99036.07 C2812 99036.07 C2812 99036.07 C2812 99036.07

C2866 99087.73 C2866 99087.73 C2866 99087.73 C3866 99097.73 02866 99087.73 C2866 99087.73 C2866 99087.7 3 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73 C2866 99087.73

C3967 99075.38 C2967 99075.28 C2867 99075.28 C2867 99075.28 C2867 99075.28 C2867 99075.28 C2867 99075.28 C2867 99075.28 C2867 99075.39 C2867 99075.29 C2967 99075.28 C2867 59075.28 C2867 99075.29 C2867 99075.28 C2S67 95075.28 C3867 95075.28

C2868 85085.10 C2868 99085.10 C2868 99085.10 C3868 99085.10 C3868 99085.10 C3868 99085.10 C3968 99095.10 C3868 99085.10 C2868 95085.10 C3868 55085.10 C3866 85085.10 C2868 99085.10 C2868 99085.10 C3863 99085.10

C2869 99071.06 C2869 99071.06 02869 99071.06 C2969 99071.06 C2869 95071.06 C2869 99071.06 C2969 99071.06 C2869 99071.06 C2969 59071.06 C2969 99071.06 C2869 99071.06

195294.34 SNDT11091 195294.34 SNDT11092 195294.34 SNCH11093 195294.34 SNCM11094 195394.34 SNCM1109S 195294.34 SNCM11096 155394.34 SNCM11097 195294.34 SNCM11099 195394.34 SNCH11099 195294.34 SNO411100 195294.34 SNCH11101 195294.34 SNCM11102 195294.34 SNDB11103

195355.97 SNDT1U04 195355.97 SNDT11105 195355.97 SNDT11106 195355.97 SNDT11107 195355.97 SNCMD1106 195355.97 SNCHD1107 195355.97 SNCM11109 195355.97 SNCH11109 195355.97 SNCM11110 195355.97 SHCM11111 195355.97 SNCM11U2 195355.97 SNCH11113 195355.97 SNCH11114 135355.97 SNCM11115 195355.97 SHCM11116 195355.97 SNCM11117 195355.97 SNCM11118 195355.97 SNCM1111S 155355.97 SNDB11120

195841.73 SNDT1112S 195841.73 SNCM11126 195841.73 SNCM11127 195841.73 SNCH11128 195841.73 SNCH11129 195841.73 SNCM11130 195841.73 SNDB11131 195841.73 SNDBD1131 195841.73 SND811132 195841.73 SN 11133

195239.59 SN 11320 195229.58 SN 11321 195239.59 SN 11332 155339.58 SN 11333 195229.58 SN 11324 195229.58 SN 11325

195293.38 SNDT11364 195253.38 SNCM113 6S 185353.38 SNCM89002 195293.38 SNCM11366 195393.38 SNCM11367 195393.38 SNCH11368 195353.38 SNCH11369 195393.38 SNCM11370 195393.39 SNCH11371 135293.38 SNCM11373 195293.38 SNDB11373

195273.63 SNDT11374 195373.63 SNDT11375 195272.63 SNDT11376 195372.63 SNCM11377 195273.63 SNCM11378 195373.63 SNCM11379 195373.63 SNCH11380 196373.63 SNCM113 81 195373.63 SNCM11383 195373.63 SNCM11393 195272.63 SNDBD1383

195328.05 SNDT11384 195339.05 SNDT11385 195338.05 SNDT11386 155328.05 SNCH11387 155338.05 SNCM11388 195338.05 SNCM11389 195338.05 SNCM11390 195338.05 SNCM11391 195328.05 SNCH11393 195338.OS SNCM11393 195338.05 SNCM11394 195338.05 SNDB11395 195339.05 SNDBD1395

195317.09 SNDT11396 195317.09 SNDT11397 195317.09 SNDT11398 195317.09 SNDT11399 195317.09 SNDT11400 195317.09 SNCM11401 195317.09 SNCM11402 195317.09 SNCH11403 195317.09 SNCM11404 195317.09 SNCH11405 195317.09 SNCM11406 195317.09 SNCM11407 195317.09 SNCM11408 195317.05 SNCMH409 195317.09 SNCM11410 195317.05 SNCH11411 155317.09 SNDB11412

195311.45 SNDT11413 195311.45 SNDT11414 195311.45 SNDT11415 195311.45 SNDT11416 195311.45 SNDT11417 155311.45 SNCH11418 195311.45 SNCM11419 195311.45 SNCH11420 195311.45 SNCH11421 195311.45 SNCM11432 135311.45 SNCH11423 135311.45 SNCM11424 135311.45 SNCH1142S 195311.45 SNCM11436 195311.45 SNCM11437 195311.45 SNDB11438

195305.38 SNDT11429 195305.38 SNDT11430 195305.38 SNDT11431 195305.38 SNDT11432 195305.38 SNDT11433 196305.38 SHCM11434 195305.39 SHCH11435 195305.39 SNCH11436 195305.38 SNCM11437 195305.38 SNCM11438 195305.38 SNCM11439 195305.39 SNCM11440 135305.38 SNCM11441 155305.38 SNDB11442

155299.06 SNDT11443 195295.06 SNDT11444 195299.06 SNDT1144S 195299.06 SNDT11446 195399.06 SNDTU447 195399.06 SNDT11448 196299.06 SNCH11449 195299.06 SNCM114S0 195299.06 SNCM11451 195299.06 SNCH11452 195299.06 SNCM11453

7.780 9.390 8.960 9.530 10.620 11.130 11.530 12.040 13.640 13.310 13.690 13.870 14.180

15.370 15.410 16.030 16.580 16.580 16.580 16.980 17.530 18.380 19.070 19.730 30.110 31.000 21.750 22.420 22.870 23.610 34.330 24.510

11.040 11.140 12.130 13.600 15.310 16.210 16.860 16.860 17.150 17.710

43.360 43.360 43.520 44.520 16.160 17.310

6.460 6.560 7.180 7.570 8.590 9.400 10.470 11.830 12.830 13.S80 14.060

10.550 10.650 11.340 11.510 12.300 13.550 14.650 15.790 16.650 17.590 18.380

9.930 10.030 10.620 10.780 11.700 13.100 14.110 14.680 15.570 16.610 17.700 18.430 18.430

3.310 3.410 3.670 3.780 1.260 4.440 4.950 5.310 6.050 6.550 7.620 8.370 8.500 9.600 11.020 11.110 11.370

6.620 6.720 7.040 7.150 7.560 7.790 9.520 9.300 10.430 11.240 12.150 12.860 13.740 14.060 14.180 14.390

4.930 1.930 5.190 5.280 5.660 5.820 6.320 7.320 8.740 9.590 11.300 12.170 12.270 12.590

8.480 8.630 8.780 8.940 9.210 9.430 9.650 10.420 11.100 12.000 12.940

8.380 8.360 9.530

10.630 11.120 11.520 13.040 13.640 13.310 13.680 13.830 14.180 14.230

15.410 16.030 16.590 16.380 16.680 16.680 17.520 18.280 13.070 13.730 20.110 21.000 21.750 22.420 33.870 33.610 34.330 34.510 24.600

11.140 12.120 13.600 15.210 16.310 16.860 17.150 16.560 17.710 17.810

43.360 43.520 44.520 46.160 17.310 17.4X0

6.560 7.180 7.570 8.590 9.400 10.470 11.830 12.830 13.580 14.060 14.160

10.650 11.340 11.510 12.300 13.560 14.650 15.790 16.650 17.590 18.470 18.520

10.020 10.620 10.780 11.700 13.100 11.110 14.680 15.570 16.610 17.700 18.430 18.530 18.530

3.410 3.670 3.780 4.260 4.440 4.990 5.330 6.050 6.950 7.620 8.370 8.900 9.600 11.020 11.110 11.370 11.500

6.730 7.040 7.160 7.560 7.790 8.530 9.300 10.430 11.340 13.190 12.860 13-710 14.060 14.180 14.390 14.490

4.930 5.150 5.290 5.660 5.820 6.320 7.320 8.740 9.680 11.300 12.170 12.270 12.580 12.680

8.630 9.780 8.910 9.210 9.430 9.650 10.420 11.100 11.980 12.840 13.750

1.39 1.38 1.29 1.32 1.39 1.30 1.31 1.35 1.35 1.33 2.45 1.31 2.52

2.19 1.59 1.39 3.46 3.46 2.46 1.39 1.29 1.29 1.29 1.29 1.29 1.29 1.30 1.29 1.28 1.27 1.34 2.42

1.71 1.30 1.29 1.29 1.30 1.29 2.S4 2.54 1.35 3.62

2.40 1.35 1.33 1.33 1.34 2.22

2.49 1.34 1.67 1.31 1.31 1.30 1.30 1.31 1.25 1.37 2.S6

2.39 1.32 2.25 1.34 1.30 1.29 1.31 1.31 1.30 1.33 2.00

1.87 1.32 1.67 1.32 1.32 1.30 1.35 1.31 1.30 1.29 1.32 2.16 2.00

2.30 1.40 2.10 1.30 2.30 1.30 1.30 1.30 1.30 1.30 1.30 1.30 1.30 1.30 2.10 1.40 2.20

2.50 1.40 2.20 1.30 2.30 1.30 1.30 1.30 1.30 1.30 1.30 1.30 1.30 1.80 1.40 2.40

2.40 1.40 1.90 1.34 2.10 1.40 1.30 1.30 1.40 1.40 1.30 1.80 1.40 2.40

1.70 1.40 1.80 1.40 2.17 1.50 1.41 1.40 1.40 1.40 1.40

13.20 12.50

.60 1.40 9.50 .20 .40

2.80 1.60 5.10 82.30 8.60 87.20

72.30 31.30 2.60 81.60 81.60 81.60 13.10

.60

.SO

.20

.40

.30

.30

.30

.40

.50

.80 9.90 81.60

44.30 1.20 .20 .30 .60 .60

85.60 85.60 8.70 88.80

69.70 5.80 2.80 3.30 3.20

69.30

83.10 6.30 39.10 1.90 .60 .40 .60

1.40 1.80 12.40 84.00

78.90 4.30

70.80 7.00 .50 .30

1.00 .40 .30

7.50 85.00

53.80 4.10 39.10 3.30 1.30 .10

4.30 1.30 .40

1.90 S.36

67.43 95.00

76.40 14.60 66.20 1.40

73.30 1.90 1.10 .20 .10 .10 .70 .20 .80 .SO

66.00 8.00

70.40

83.00 14.30 71.50 3.40

73.50 6.70 .40 .01 .20 .20 .30 ,50

3.90 45.80 11.70 79.10

90.20 13.70 52.70 3.30

66.10 11.30

.70

.30

.30

.70 5.60 46.00 4.50

79.50

40.50 9.60 17.00 7.20 68.12 11.40 1.09 1.70 .40 .03 .10

4.40 4.20 4.70 5.10 4.90 5.10 5.40 5.30 6.30 4.40 2.90 4.00 2.30

2.80 4.10 1.10 3.30 3.30 3.30 1.00 4.60 4.60 1.60 1.30 1.80 4.60 4.60 4.00 4.00 3.70 3.10 2.90

2.00 4.60 5.10 4.90 4.60 1.10 2.30 2.30 1.50 2.10

4.10 6.80 7.10 7.10 7.40 4.70

3.60 4.70 3.90 5.10 5.60 5.10 5.30 4.80 4.40 4.40 3.60

3.40 4.SO 4.60 4.40 5.10 S.30 5.00 S.30 4.70 4.20 1.30

3.70 4.60 3.90 4.90 5.40 5.60 5.10 S.40 5.00 4.60 4.60 4.59 1.30

3.40 4.70 3.60 4.70 4.30 5.20 5.40 5.80 5.60 5.40 5.20 5.SO 5.00 S.40 4.40 4.40 4.00

3.30 4.40 3.SO 4.60 4.10 4.90 5.20 5.50 S.30 S.30 4.90 4.30 4.30 1.30 4.30 4.10

3.50 4.60 4.20 6.20 4.70 6.00 1.00 9.00 9.10 7.90 4.10 3.90 9.60 3.20

4.10 5.60 4.90 S.50 5.41 9.20

10.14 10.10 10.20 8.80 9.10

ASH MOIS VM CV SULPHUR

.37

.37

.28

.32

.56

.33

.37

.71 1.50 .65

.26 .11

.19 .34 .24 .31 .31 .31 .37 .27 .34

.28

.27

.34

.25

.31

.36

.63

.50

.23

.29

.18

.18

.19

.24

.25

6.48 2.74 1.64 .75 .85 .58

.13 .41

1.27 .47 .63 .46 .35

1.11 .37 .36 .46

.13 .38 .50 .34 .19 .17 .19 .32

.92 1.07 1.27 .59

1.30 .28

2.23 1.08 .45 .48 .29 .31 .31

.90

.90

.60

.60

.30

.30

.40

.30

.20

.50

.20

.20

.30

.30

.40

.30

.30

.40

.60

.20

.20

.20

.20

.30 1.70 .30 .30

.40 .50 .40 .50 .22 .70 .67 .50 .50 .SO .50

DDH EASTINO NORTHINO SAMP. No. DEPTOP DEPBOT RD ASH MOIS VH CV SULPHUR

C2869 C3969 C2869 C2869 C3869

C3915 C391S C2915 C391S C3915 C3915 C2315 C2315 C2915 C2315 C2915 C2915 C2915 C2915 C2915 C3915 C2915

C2916 C2916 C2916 C3914 C2316 C3316 C3316 C2916 C2916

C2317 C3917 C3917 C3917 C3917 C3317 C3917 C3917 C2917 C2317 C2917 C2917 C2317 C2S17

C2918 C2918 C2918 C2318 C2919 C2918 C2318 C2918 C2918 C2918

C2915 C3519 C2919 C3919 C3919 C3919 C2319 C2919 C3919 C2919 C2919 C2919 02919 C2S19 C3919

C2920 C2920 C2920 C2920 C2320 O2920 C2920 C2920 C2920 C2920

C2921 C2921 C2921 C2921 C2321 C2921 C2921 02921 C2931 C2931

C3922 C3933 C2322 C2922 C2922 C2922 C2922 C2922 C2922 C2322 C2322 C2922 C2933

C2923 C2923 C2923 C3333 C3933 C3933 C2933 C2923 C2923 C3333 C2923 C2923

C2924 C2924 C2934 C2324 C3534 C3934 C2924 C2924 C2924 02924

C252S C293S C2925 C232S C2325 02925 C293S C393S 0393S

C3926 C2926 C2926 C2526 C2526

53071.06 99071.06 99071.06 99071.06 99071.06

98777.81 98777.81 98777.81 98777.81 88777.81 98777.81 98777.81 58777.81 88777.81 88777.81 98777.81 98777.81 98777.81 98777.81 98777.81 98777.81 98777.81

98726.09 98726.09 98736.09 98726.09 98736.09 99736.09 98726.09 98726.09 98726.09

98469.41 98469.41 98469.41 98469.41 98463.41 58469.41 58469.41 99469.41 98469.41 99469.41 98469.41 99469.41 98469.41 99469.41

98S06.21 98506.21 88506.21 98506.21 98506.21 98506.31 98506.31 98506.31 98506.21 96506.21

98532.18 58532.18 98533.18 98533.18 98533.18 98533.18 98533.18 98533.18 99S33.19 98533.18 98532.1S 98532.18 98532.19 98532.18 99532.19

98360.91 98360.91 99360.91 98360.91 98360.91 99360.91 99360.91 98360.91 98360.91 99360.91

99431.99 99431.98 98431.88 98431.38 98431.88 99431.88 98431.88 98431.88 98431.88 98431.88

98194.13 98194.13 98194.13 98194.13 98194.13 98194.13 98194.13 98194.13 99194.13 98154.13 99194.13 98191.13 98194.13

99390.44 98380.44 98380.44 98380.44 98380.44 98380.44 58380.44 98390.44 58380.44 58380.44 98380.44 99380.44

98725.57 88725.57 98725.57 98725.57 98725.57 987 25.57 98725.57 987 25.57 987 25.57 99725.57

98450.71 98450.71 98450.71 98450.71 98450.71 98450.71 98450.71 98450.71 98450.71

99016.59 55016.59 99016.59 99016.59 99016.59

195299.06 SNCH11454 135339.06 SNCH114S5 195339.06 SNCM11456 195333.06 SNCM114S7 135333,06 SHDB11458

135351 195351 195351 195251 195251 195251 195251 195351 195351 195351 196351 195351 195251 195251 195251 195251 195251

195366 195366 195366 195366 195366 195366 195366 195366 195366

19S373 195373 195373 195373 195373 195373 195373 19537 3 195373 195373 195373 195373 19537 3 19537 3

,09 SNDT11463 .09 SNDT11464 09 SNDT11465 03 SNDT11466 03 SNDT11467 09 SNCH11468 09 SNCM11469 09 SNCH11470 09 SNCM11471 .09 SNCM11472 .09 SNCM12473 .05 SNDB11474 ,05 SNDB11475 .05 SNDB11476 ,09 SND811477 .09 SNDB11478 .09 SNDB11479

.94 SNDT11480

.94 SNCH11481

.94 SNCM11483 94 SNCM11493 94 SNCM11484 94 SNCH11485 54 SNCM11496 94 SNDB11487 94 SNDB11486

88 SNDT11489 98 SNDT11490 88 SNDT11491 88 SNCM11492 88 SNCH11433 88 SNCM11434 88 SNCM11435 88 SNDB11496 88 SNDB11497 88 SNDB11438 88 SNDB11433 88 SND811500 88 SNDB11501 88 SNDB11503

185625.16 195635.16 155625.16 195625.16 195625.16 155625.16 195625.16 195635.16 195625.16 195635.16

195766.11 195766.11 195766.11 195766.11 195766.11 195766.11 195766.11 135766.11 155766.11 155766.11 155766.11 155766.11 195766.11 195766.11 195766.11

195741.59 195741.59 195741.59 195741.59 195741.59 195741.59 195741.59 195741.59 195741.59 195741.59

195980.97 195880.97 195880.97 195880.97 195980.97 195980.87 155880.57 155880.87 19S880.97 195880.97

SNDT11504 SNCH12505 SNCM11506 SNCM11507 SNCH11508 SNCM11509 SNCM11510 SNCM11511 SNCM11512 SNDB11513

SNDT11515 SNCM11516 SNCM11S17 SNCM11518 SNCM11S19 SNCM11520 SNDB11521 SNDB11522 SNDB11523 SNDB11524 SND811525 SNDB11526 SNDB11537 SNDBU528 SNDB11523

SNDT11S30 SNCM11531 SNCM11532 SNCM11533 SNCM11534 SNCM11S35 SNCM11536 SNDB11537 SNDB11538 SNDB11539

SHDT11540 SNDT11541 SNCM11542 SNCM11543 SNCM11544 SNCM11545 SNCM11546 SNCM11547 SNCM11548 SNDB11S49

195519 195519 195513 135519 195519 195519 195515 155515 195519 19551S 195519 195515 155519

44 SNDT11550 44 SNDT11551 44 SNDT11552 44 SNDT11553 44 SNCM11554 14 SNCM11S55 41 SNCM11556 .44 SNCM11S57 14 SNCM11S59 .44 SNCH11559 44 SNCM11560 14 SNCM11561 44 SKDBU562

195128.30 195129.30 195128.30 185128.30 155128.30 195138.30 195128.30 195128.30 195138.30 195138.30 135138.30 135138.30

135124.61 195124.61 195124.61 195124.61 135124.61 195134.61 195124.61 195134.61 195134.61 195134.61

195001.56 195001.56 195001.56 195001.56 195001.56 195001,56 195001.56 155001.56 155001.56

195503.36 135503.36 195503.36 195503.36 195503.36

SNDT11S63 SNCM11564 SNCH11S65 SNCM11566 SNCM11S67 SNCM1156B SNCM11569 SNDB11570 SND811571 SNDB11572 SNDB11573 SNDB11574

SNDT11575 SNCM11576 SNCM11577 SNCM11579 SNCM11579 SNCM11580 SNCM11SS1 SNCM11S82 SNCM11583 SNDB11S84

SNDT11585 SNCM11S86 SNCH11587 SNCML1588 SNCM11589 SNCM11S90 SNCH11591 SNCH11S92 SNDB11S93

SNDT11554 SHDT11555 SNDT11556 SNDT11S97 SNCM11598

13.750 14.670 15.580 15.700 15.950

50.430 50.530 50.580 51.110 51.580 51.700 52.750 53.750 54.750 55.750 56.410 57.780 57.880 59.760 59.190 59.400 60.580

14.700 44.800 45.270 46.360 47.360 48.300 49.520 51.050 51.700

36.320 35.430 35.940 35.970 37.150 38.320 38.870 39.870 39.980 10.140 40.380 40.640 40.740 40.910

39.070 39.170 30.170 31.170 33.170 33.170 34.170 35.170 36.170 36.790

26.540 26.640 27.890 28.890 29.990 31.090 32.630 32.710 33.450 33.520 34.160 34.430 35.680 35.780 36.150

35.070 35.170 36.050 36.770 38.270 39.250 39.590 40.250 40.490 40.770

37.730 38.320 38.420 38.810 39.810 40.810 41.810 42.810 13.810 44.970

30.530 30.630 30.540 31.000 31.370 32.300 32.580 33.150 33.790 34.780 35.770 36.760 37.620

27.700 27.900 28.270 28.450 29.150 30.130 31.070 31.990 33.330 33.960 33.100 33.3S0

14.930 15.000 15.500 17.010 17.420 17.500 17.840 17.550 18.550 19.380

19.560 15.660 21.040 21.120 22.000 22.950 23.580 34.640 35.590

18.400 18.500 18.610 18.720 19.850

14.670 15.580 15.700 15.950 16.050

50.S30 50.590 51.110 51.590 51.700 52.750 53.750 54.750 S5.750 56.410 57.780 57.880 58.760 58.190 59.400 60.580 60.680

44.800 15.270 16.360 17.360 48.300 49.520 50.640 51.700 51.800

35.420 35.840 35.970 37.150 39.320 38.870 39.970 39.980 40.140 40.280 40.640 40.740 40.510 41.000

29.170 30.170 31.170 32.170 33.170 34.170 35.170 36.170 36.780 37.510

26.640 27.890 28.890 23.850 31.050 32.630 32.710 33.450 33.520 34.160 34.430 35.680 35.780 36.150 36.250

35.170 36.050 36.770 38.270 35.250 39.590 40.250 40.490 40.770 40.870

38.100 38.420 38.810 39.910 40.810 41.810 12.810 13.810 11.870 44.970

30.630 30.940 31.000 31.370 32.300 32.590 33.150 33.750 31.780 35.770 36.760 37.620 37.720

27.800 28.270 28.450 29.150 30.130 31.070 31.990 32.230 32.960 33.100 33.350 33.450

15.000 15.900 17.040 17.420 17.500 17.940 17.950 18.950 19.360 19.480

13.660 21.040 21.120 22.000 22.950 23.S90 24.640 25.580 25.680

18.500 18.610 18.720 19.950 20.400

1.30 .20 1.30 1.30 3.30 73.80 1.40 10.80 3.50 81.90

1.94 53.30 1.35 8.00 2.66 87.10 1.35 9.10 2.05 63.20 1.34 6.30 1.30 1.29 1.30 1.29 1.29

.40

.20

.10

.30 1.70

.53 84.60 1.86 52.20 1.35 8.60 2.46 80.90 1.39 13.40 2.61 95.60

2.00 59.90 1.40 13.00 1.30 1.30 1.30 1.30 1.30 1.30

.50

.50

.50 1.40 1.20

2.60 88.90

2.59 85.30 1.33 4.80 3.52 83.70 1.33 3.00 1.33 3.60 1.30 .70 1.31 .80 1.83 49.30 .36 9.90 .48 81.00 .33 7.50 .50 84.50 2.00 .29 3.00 .65 39.90

7.10 1.60 1.20 1.10 1.10

3.50 1.90 3.50 1.60 1.30 1.70 5.10 1.90 1.90 1.60 1.40 2.40 3.90 4.50 2.50 1.30 2.00

4.40 4.30 . 4.90 5.20 5.10 -5.00 -4.60 . 4.20 . 2.30 •

3.40 -4.20 . 3.70 • 1.60 -1.70 • 4.60 -5.00 -3.60 -1.50 -2.40 -3.90 -

3.70

2.59 94.40 1.35 8.00 1.30 1.30 1.30 1.29 1.30 1.30 1.30 1.70 4.60 1.62 37.40 3.10

5.10 5.00 5.50 5.30 5.20 5.50 5.20

2.55 95.30 1.41 13.90 1.34 2.70 1.30 1.00 1.31 .80 1.38 10.20 2.25 74.40 1.44 15.70 2.32 74.60 1.43 15.20 2.23 72.50 1.40 12.30 3.69 97.80 1.33 5.70 3.30 74.90

3.65 91.50 1.31 1.20

.50

.80

.60 1.00

1.29 1.40 2.24 70.50 1.34 4.50 2.38 78.10

1.46 15.90 2.64 86.00 1.42 15.00 1.29 1.10 1.30 .40 1.30 .40 1.30 .30 1.30 1.10 1.29 1.40

.30

.31

.28

3.40 4.70

4.30 2.20

2.20 4.90 5.00 4.70 4.70 4.00 4.50 2.90 4.90 2.60

4.60 3.70 4.40 4.90 5.10 5.30 4.70 4.40 4.70

2.09 63.70 3.60 -

1.95 57.50 1.31 3.60 3.05 65.20 1.35 8.60 1.31 1.60 1.31 .50 1.47 10.80 1.33 2.50 1.30 1.30 1.29 1.30 2.90 2.51 92.80

.40

.50

.70

2.17 70.30 1.30 2.50 1.33 5.30

.50

.70 1.31 1.32 2.23 73.70 1.31 4.30 1.36 11.70 1.30 3.40 2.50 80.30 4.60

3.70 4.40 3.70 4.50 S.10 5.40 1.80 5.50 5.10 4.80 4.20 4.20 2.80

3.20 4.60 5.20 5.40 5.40 5.30 S.10 2.70 4.30 3.60 4.10

1.75 51.20 1.33 1.60 1.33 1.90 1.33 3.70 1.46 21.10 1.31 5.20 2.09 64.90 1.31 2.20 1.32 1.90 2.40 73.90

2.55 31.60 1.31 1.S0 1.45 18.00 1.30 1.20 1.28 .60 5.00 1.29

2.60 5.60 5.40 5.50 4.10 4.70 4.10 5.00 5.00 2.70

3.00 5.30 5.20 5.50

1.29 2.50 93.20

2.21 73.60 1.11 14.70 1.57 30.90 1.31 .90 1.31 .70

.40 4.90 -

3.20 3.40 4.10 4.90 5.50

.60

.30

.30

.30 1.10

.19 .28 .20 .25 .17 .25 .27 .22 .21 .19 .20 .36 .33 .37 .21 .48

.18

.33

.32

.23

.21

.18

.18

.22

.38

.24

.49

.07

.22

.17

.16

.16

.19

.14

.21

.19

.22

.25

.16

.15

.16

.13

.16

.08

.28

.16

.15

.15

.22

.18

.39

.18

.29

.19

.16

.16

.19

.21

.26

.41

.27

.18

.15

.15

.32

.93

.16

.13

.16

.16

.16

.13

.20

.20

.21

.21

.30

.44

.23

.24

.31

.27

.23

.24

.24

.17

.24

.35

.22

.34

.23

.22

.26

.37

.53

.21

Appendix 6.7 (cont'd)

DDK EASTING

C2926 33016.53 C2926 99016.59 C2926 99016.59 C3926 99016.59 C3936 99016.59 C2936 99016.59

C2943 101239.44 03942 101239.44 03943 101239.44 C3942 101239.44 C3943 101239.44 C2943 101239.44 C2943 101239.44

C2S44 101746.43 C2944 101746.49 C3544 101746.49 C3944 101746.49 C3944 101746.49 C3344 101746.49

C2992 96488.47 C3983 96488.47 C3983 96488.47 C3S93 96488.47 C2982 36488.47 C2983 36498.47 C2383 96489.47 C3983 36488.47 C3983 96488.47

C2384 36192.38 C2984 96192.38 C3384 36183.38 C3984 96183.39 C2994 96183.39 02584 96182.38 C3984 96183.38 C3994 96183.38

C398S 56805.49 C3995 96905.49 C2985 96805.49 C3985 96805.49 C3995 36805.49 C3985 96805.49 C3985 96805.49 C399S 96805.49 C2985 96805.49

C2994 9914S.32 C3994 99145.32 C2934 35145.32 02554 35145.32 C2994 55145.32 03991 99145.33 C2994 99145.32 C2994 99145.32 C2994 99145.32 C2994 99145.32 C2994 99145.32 C2994 99145.32 02994 99145.32 02994 95145.32

C2995 99990.72 C2995 98990.72 C2595 98990.72 C2995 59990.72 C299S 98990.72 C299S 99990.73 C3995 98990.73 C3995 99990.73 C29S5 98990.72 C2995 99990.72 C2995 99990.72 C2995 58590.72 C2995 58590.72

C2996 99047.45 C2996 990 47.45 02996 99047.45 C2996 99047.45 C2996 99047.45 C2996 99047.45 02996 99047.45 C2996 33047.45 02996 99047.45 C2996 99047.45 C2996 99047.45 C2996 95047.45

C3000 56615.33 C3000 36615.53 C3000 96615.93 C3000 56615.93 C3000 96615.93 C3000 96615.93 C3000 96615.93 C3000 96615.93 C3000 96615.93 C3000 96615.93 C3000 96615.93 C3000 96615.93 C3000 96615.33 C3000 96615.93 C3000 96615.93 C3000 96615.93

C3001 96277.19 C3001 96277.19 C3001 96277.19 C3001 96377.19 C3001 96377.19 O3001 96277.19 C3001 96277.19 C3001 96277.19 C3001 96377.19

C3003 96735.64 O3003 96735.64 C3003 96735.64 C3002 96735.64 C3O02 96735.64 C3002 96735.64 03002 96735.64 C3002 96735.64 C3002 967 35.64

C3002 56735.64 C30O2 56735.64 03902 96735.64 C3002 567 35.64 03002 56735.64 C3002 96735.64 03002 56735.64

G3003 96399.35 C3003 36399.95 C3003 96399.35 C3003 96339.95 O3003 96399.95 C3003 96399.95 O3003 96399.35 C3003 36399.35 C3003 96399.35 C3003 36399.35 C3003 36393.55 C3003 36393.55 C3003 96393.35

NORTHING SAMP. No.

135503.36 SNCM1153S 195503.36 SNCM11600 135503.36 SNCM11601 I95S03.36 SNCM11602 195503.36 SNCM11603 195503.36 SNDB11604

195215.77 SN 11634 195215.77 SN 11635 195315.77 SN 11636 195315.77 SN 11637 195315.77 SN 11638 135315.77 SN 11639 195315.77 SN 11640

194996.30 SN 11647 194996.30 SN 11648 194996.20 SN 11649 194996.30 SN 11650 194996.30 SN 11651 194996.30 SN 11652

194538.25 SNDT11744 134538.25 SNCM1174S 194538.35 SNCH11746 134598.25 SNCM11747 194S98.25 SNCM11748 194598.25 SNOM11749 194599.35 SHOM11750 194599.35 SNDB117S1 194598.35 SNDB11753

195135.97 SNDT11770 195135.97 SN0H11771 195125.97 SNCM11772 195125.97 SNCH11773 195125.97 SNCM11774 195125.37 SNCH11775 195125.97 SNCH11776 195125.97 SNDB11777

195046.03 SNDT11783 135046.03 SNCM11784 135046.09 SNCM11785 135046.03 SNCM11786 13S046.05 SNCM11787 135046.03 SNCM11788 195046.09 SNCM11789 195046.09 SNCM11790 195016.09 SND81I791

195339.09 SNDT11606 195339.09 SNDT11807 195339.09 SNDT11S08 195339.09 SNCM11809 195335.05 SNCM11810 195339.09 SN0M11811 195339.09 SNCM11812 195339.03 SNCH11S13 135339.09 SNCM11814 195339.09 SNCM11815 195339.05 SNCM11816 195339.05 SNCM11817 195339.09 SNDB11B1S 195339.09 SNDB11819

195434.44 SNDT11932 195434.44 SNCM11833 195434.44 SNCH11834 195434.44 SNCM11S35 135434.44 SNCM11836 135434.44 SNCM11837 195434.44 SNCMU838 195434.44 SNDB11839 195434.44 SNDB11840 155434.44 SNDB11841 195434.44 SNDB11842 195434.44 SNDB11843 195434.44 SNDB11844

195453.83 SNOT11845 135453.33 SNOM11846 135453.83 SNCM11847 155453.83 SNCM11848 195453.83 SNCM11843 195453.83 SNCM11850 195153.83 SNCH1I35I 195453.83 SNDS11852 195453.83 SNDB11S63 135453.83 SNDB11854 135453.33 SNDB11855 135453.83 SNDB11856

135245.55 SNDT11871 195245.55 SNCM11872 195245.95 SNOH1187 3 155245.95 SNCM11874 195345.95 SNCM11875 195345.95 SNOM11976 195345.95 SNCM11977 195245.35 SNCM11878 195345.95 SNCM11879 135345.35 SNCM11880 135345.35 SNCM11881 195345.95 SNCM11983 195245.95 SNCM11883 195245.55 SNCM11884 195245.35 SNCM11885 195245.95 SNDB11986

195457.41 SNDT11898 1954S7.41 SNDT11899 195457.41 SNDT11300 135457.41 SNDT11301 195457.41 SNCM11902 195457.41 SNCM11903 195457.41 SNCM11904 195457.41 SNCH11905 195457.41 SNDB11906

195382.35 SNDT11907 195383.35 SNOM11908 195392.25 SNCM11909 195332.25 SNCM1I9I0 195382.35 SNCM11311 155383.35 SNOM11312 135382.25 SNCH11913 135382.25 SNCM11314 135382.25 SNOH11315

135382.25 SNCM11916 195392.25 SNOM11917 195382.25 SNCM11918 155382.25 SNCM11919 195382.35 SNCM11930 195383.35 SNDB11331 195393.35 SNDBL1922

195753.13 SNDT11939 195753.13 SNDT11940 195753.13 SNDT11941 195753.13 SNDT11942 135752.13 SNCM11343 135752.13 SNCM11944 135752.13 SNCM1134S 155752.13 SNCM11S46 155752.13 SNCM11347 135752.13 SNCM11948 195753.13 SNCM11949 195753.13 SNCM11350 135753.13 SNDB11351

DEPTOP

30.400 31.530 32.3SQ 33.430 34.170 34.850

53.130 53.330 59.910 60.780 61.300 61.960 63.660

54.710 54.810 55.700 56.630 57.350 58.360

31.320 31.330 32.460 33.470 34.580 35.750 37.290 38.330 39.310

57.7 30 57.780 53.210 60.630 61.460 62.320 63.250 64.420

53.770 54.150 55.450 56.700 58.130 59.550 60.800 62.200 63.680

.100

.300 1.130 1.480 1.580 3.080 4.550 5.160 5.310 5.620 6.850 7.360 8.300 3.070

13.380 15.540 21.050 22.060 23.030 24.220 35.530 36.050 36.130 36.300 36.630 36.310 37.050

17.400 17.500 18.300 19.580 21.150 22.160 22.240 23.120 23.330 23.560 33.840 34.300

50.820 50.920 51.540 52.330 53.000 53.930 54.700 55.600 56.580 56.720 57.770 58.240 58.370 53.340 60.230 61.400

81.740 81.840 82.600 83.750 84.040 84.900 85.360 86.320 88.140

33.180 33.280 34.330 35.680 35.820 37.000 37.330 39.140 39.980

40.750 11.840 43.990 43.800 44.350 15.080 15.780

140.710 110.810 141.030 141.130 143.180 143.080 144.070 144.340 145.450 146.330 147.460 148.690 149.310

DEPBOT

31.530 33.350 33.430 34.170 34.950 24.350

59.390 59.910 60.780 61.300 61.960 63.660 63.760

54.810 55.700 56.620 57.350 58.360 58.460

31.320 32.460 33.470 34.580 35.750 37.290 38.330 39.310 33.430

S7.7 80 53.310 60.630 61.460 62.320 63.250 64.420 64.530

54.150 55.450 56.700 58.130 53.550 60.300 63.300 63.680 63.760

.300 1.130 1.480 1.380 3.080 4.550 5.160 5.310 5.630 6.850 7.360 8.300 9.070 9.600

15.540 21.050 22.060 23.030 24.220 25.530 26.050 26.120 26.300 26.620 26.310 27.050 37.120

17.500 19.200 19.990 21.150 22.160 22.240 23.120 23.330 23.560 23.940 24.200 24.300

50.920 51.540 52.320 53.000 53.530 54.700 55.600 56.580 56.720 57.770 58.240 58.370 59.340 60.390 61.400 61.500

81.940 82.600 83.750 84.040 84.900 85.960 36.920 88.140 88.240

33.280 34.490 35.680 35.820 37.000 37.930 39.140 39.980 40.750

41.840 42.880 43.800 11.850 15.080 45.780 45.880

140.810 141.030 141.130 143.180 143.080 144.070 144.340 145.450 146.330 147.460 148.6 90 149.910 150.010

RD

1.30 1.31 1.31 1.31 1.41 3.54

1.53 1.33 1.31 1.37 1.33 1.34 3.06

3.21 1.34 1.30 1.31 1.37 1.59

3.03 1.31 1.31 1.30 1.31 1.31 1.33 1.32 2.31

1.52 1.32 1.31 1.31 1.31 1.34 1.31 2.49

1.81 1.31 1.31 1.30 1.31 1.30 1.31 1.31 2.72

2.28 1.43 1.47 1.43 1.35 1.34 1.32 2.50 1.42 1.31 1.31 1.32 1.87 1.36

1.66 1.30 1.30 1.29 1.30 1.32 1.31 2.39 1.27 2.04 1.28 1.65 2.51

2.48 1.38 1.31 1.30 1.31 2.11 1.30 1.61 2.61 1.30 1.47 2.28

2.28 1.34 1.31 1.30 1.30 1.37 1.32 1.30 1.58 1.30 1.29 1.6S 1.31 1.32 1.30 2.47

2.64 1.29 1.30 2.SI 1.31 1.30 1.31 1.33 2.20

1.93 1.31 1.29 I.so 1.30 1.31 1.30 1.30 1.33

1.29 1.29 1.29 1.32 1.25 1.37 2.44

2.13 1.42 2.26 1.32 1.30 1.31 2.21 1.30 1.29 1.30 1.30 1.30 1.98

ASH

.60

.50

.60 1.80 17.20 84.80

23.30 3.90 1.60 8.00 .70

3.10 58.70

68.80 8.00 3.00 3.60 1.20 32.70

57.20 .90 .40 .40 .50

1.10 1.50 1.80 72.50

20.80 .80 .50 .40

2.20 2.20 1.00 83.10

17.90 1.70 2.20 .40

1.30 .30 .50

1.80 91.20

53.90 4.60 15.30 8.20 .50

1.50 .91

95.20 9.90 .60

1.40 2.80 50.20 9.70

38.00 2.20 .40 .20 .60

2.10 3.70 80.20 1.60 62.70 1.10

34.90 83.70

92.20 9.80 .65 .80

1.10 63.90 .SU

33.70 84.50 3.30 21.20 74.40

69.30 3.20 1.20 .40

1.20 4.60 1.60 1.80

16.30 .40 .30

18.90 1.30 .50 .70

83.90

84.20 .80

1.60 78.80 1.70 .50

2.80 3.60

73.SO

52.40 4.20 1.30 32.90 1.40 1.70 2.80 1.10 3.40

.30

.40

.30 3.80 2.10 12.70 83.80

67.00 16.00 77.60 2.60 .70

5.70 74.40 1.50 .50

2.40 .80

1.30 56.20

MOIS VM CV SULPHUR

5.30 -5.40 -S.30 -4.60 -3.80 -2.10 -

4.20 -5.90 -6.20 -6.30 -7.30 -7.40 -5.10 -

4.50 -5.50 -6.90 -7.50 -7.40 -6.50 -

3.40 -5.50 -6.70 -6.10 -6.70 -6.60 -6.80 -6.30 -4.60 -

4.50 -6.40 -6.80 -6.90 -6.90 -6.70 -6.70 -3.60 -

3.50 -4.30 -4.70 -5.90 -S.70 -5.80 -5.70 -5.30 -1.70 -

12.50 -11.50 -7.30 -8.30 -7.50 -7.20 -5.56 -3.30 -7.SO -6.30 -5.70 -S.30 -4.30 -4.50 -

3.90 -4.40 -5.00 -4.60 -4.90 -4.50 -4.50 -2.30 -3.50 -2.70 -4.30 -3.90 -2.20 -

3.70 -4.40 -4.80 -5.00 -4.70 -4.10 -4.70 -3.90 -2.20 -4.00 -4.00 -2.30 -

3.30 -5.10 -5.60 -5.90 -5.90 -6.00 -6.30 -5.90 -4.30 -6.40 -6.80 -4.70 -6.40 -6.40 -5.50 -2.50 -

3.00 -5.60 -6.60 -3.00 -6.60 -S.50 -6.80 -7.00 -4.80 -

3.50 -5.SO -6.20 -6.80 -6.70 -S.60 -6.30 -6.10 -5.80 -

6.50 -6.00 -6.10 -5.50 -3.30 -4.50 -2.30 -

3.00 -

4.00 -5.10 -5.40 -5.90 -5.50 -4.80 -6.80 -6.50 -6.SO -6.40 -6.SO -4.30 -

.18

.15

.14

.15

.17

.21

4.04 2.30 1.55 .71 .79 .38

1.34

5.22 2.33 1.13 .49 .62 .89

4.20 1.9S .80 .41 .42 .28 .36

4.57 .28

4.37 1.98 .44 .29 .26 .24 .36 .39

1.64 1.51 .48 .23 .20 .26 .32 .24

1.38

.19

.48

.35

.34

.24

.26

.35

.70

.49

.47

.68 1.56 1.60 .46

.35

.24

.32

.20

.16

.16

.18

.22

.15

.18

.19

.23

.20

.15

.49

.20

.16

.15

.19

.14

.17

.18

.19

.23

.19

4.70 2.27 1.31 .48 .27 .16 .13 .14 .09 .14 .14 .10 .12 .14 .22 .23

6.09 1.44 .66 .23 .37 .28 .23 .21 .24

6.66 1.50 .93

1.55 .32 .21 .25 .18 .14

.16

.20

.19

.15

.12

.19

.31

4.72

2.95 .31

1.76 .59 .41 .14 .18 .14 .15 .13 .17 .22

DDH EASTING

C3004 56675.24 C3004 96675.24 C3004 96675.21 C3004 96675.24 C3004 36675.24 C3004 56675.24 C3O04 36675.24 C3004 56675.24 C3004 56675.34 C3004 96675.34 C3004 96675.34 C3004 96675.31 C3004 96675.34 C3004 36675.34 C3004 36675.34 C3004 36675.24

C3005 36806.03 C3005 36806.03 C3005 36806.03 C3005 96806.03 C3005 36806.03 C300S 96806.03 C3005 96906.03

C3006 96966.24 C3006 96966.24 C3006 96966.24 C30O6 96966.24

C3007 96966.18 C3007 96966.19 C3007 96566.19 C3007 56366.18 C3007 36966.19 C3007 96966.18 C3007 96966.18 C3007 96966.18 C3007 96966.18 C3007 96966.18 C3007 96966.38 C3007 96966.19 C3007 96566.18 O3007 36566.18

C3015 57825.75 C3015 57825.75 C301S 97829.75 C3015 97829.75 C3015 97829.75 C3015 97839.75 C3015 97839.75 C3015 97839.75 C3015 97829.75

C3016 98015.11 C3016 98015.11 C3016 98015.11 C3016 99015.11 C3016 98015.11 C3016 98015.11 C3016 88015.11 O3016 88015.11 03016 88015.11 C3016 98015.11 C3016 98015.11 03016 98015.11 03016 99015.11

C3017 98389.35 C3017 98389.35 C3017 98389.35 C3017 98388.35 C3017 58388.35 O3017 58389.35 03017 98389.35 C3017 98389.35 C3017 98389.35 C3017 98389.35

C3019 97580.88 C3019 97580.88 C301S 57580.88 C3018 57580.88 O3019 97580.88 C3019 97580.88 O3019 97580.88 C3019 97580.88 C3019 97580.88

C3020 97740.95 C3020 977 40.95 C3020 57740.55 C3020 57740.95 C3030 97740.95 O3030 977 40.SS C3030 37740.55 C3020 57740.55 C3020 97740.95 C3020 97740.95 C3020 97740.95 C3020 97740.95 C3020 97740.95 C3020 977 40.95 C3020 97740.55 C3020 97740.95 C3030 97740.95

C3031 97760.93 C3031 97760.92 C3021 97760.92 C3021 97760.92 C3021 97760.92 C3021 37760.92

C3022 98021.30 C3023 98031.30 C3033 98031.30 C3033 98031.30 C3033 99031.30 C3033 98031.30 C3033 99031.30 O3032 98021.30 C3022 99021.30

C3029 37224.10 O3023 37224.10

C3031 97651.76 C3031 97651.76 C3031 97651.76 O3031 57651.76 C3031 97651.76 C3031 97651.76 C3031 97651.76 C3031 97651.76 C3031 97651.76

C3032 97526.21 O3032 57926.21 C3032 97926.21 03032 97526.22 C3032 97926.31 O3033 97936.31

C3037 97457.63 C3037 37467.63 C3037 37457.63 C3037 37457.63 03037 37457.63 03037 97457.63

NORTHING

195743.37 195742.27 195742.27 195742.27 135743.37 135743.37 155743.37 155743.37 155742.27 155742.27 195742.27 195742.27 195742.27 195742.27 195742.27 195742.27

195761.20 195761.20 195761.20 195761.20 155761.20 155761.20 195761.20

195487.09 195487.09 195487.09 195497.09

195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56 195359.56

194311.34 194311.34 194311.34 154311.31 194311.34 194311.34 194311.34 194311.34 194311.34

154496.70 154496.70 194496.70 194496.70 194496.70 194496.70 194496.70 194496.70 194496.70 194496.70 194496.70 194496.70 194436.70

134517.13 194517.13 194517.13 194517.13 194517.13 194517.13 194517.13 194517.13 134517.13 154517.13

154457.94 194497.94 194497.94 194497.54 154457.54 194497.94 194497.94 194497.94 154497.94

194775.72 194775.72 194775.72 134775.72 134775.72 194775.72 134775.73 194775.72 194775.72 194775.72 194775.72 194775.72 194775.72 154775.72 194775.72 194775.72 194775.72

195013.95 155013.55 195013.95 195013.95 195013.95 195013.95

194867.52 194867.52 194867.52 194967.53 194967.53 184867.53 194967.53 134867.52 194867.53

195376.37 195376.37

195194.00 195194.00 195194.00 195194.00 195194.00 195194.00 195194.00 195194.00 155194.00

195343.91 195343.91 195343.91 195343.91 195343.91 195343.91

195373.78 195372.78 195272.78 19S272.78 195272.79 195272.79

SAMP. No.

6NDTU974 SNCM11375 51*301976 SNCM11977 SNCM11979 SNCM11379 SNCM11580 SNCM11581 SNCM11583 6NCM11S83 SNCH11S84 SNCM11S85 6NCM11S86 SNCM11987 SND811988 SNDB11989

SNDT11958 SNCM11599 SNCH13000 SNCM13001 SNCM13003 SNCM13003 SNDB13004

SNDT13009 SNCM12010 5NDB13017 SNDB13018

SNDTI2019 SNCK12020 SNCM12021 SNCM12022 SNCM12023 SNCM12024 SNCM12025 SNCM12026 SNCH12027 SHCM22029 SNCM12029 5NDB12030 SHDB12031 SNDB12032

SNDT120 40 SNCM12041 SNCM3.2042 SNCH12043 SNOM12044 SNCH12045 SNCH12046 SNCM12047 SNDB12048

SNOT12076 SNDT12077 SNDT13079 SNCM12079 6NCH12080 SNCM12081 SNCM12082 5NCM12083 SNCM12084 SNCM1208S SNCM12086 SNCM12087 SNDB12098

SNDT12094 SNDT12095 5NDT12096 SNCM12097 SNCM12098 SNCM12099 SNCM12100 SNCM12101 SNCM12102 SND812103

SNDT12137 SNCH12138 SNCM12139 SNCM12140 SNCM12141 SNCM12142 SNCM12143 SNCM12144 SNDS12145

SNDT12163 SHDT12164 SNDT12165 SNDT12166 SNDT12167 SNCM12168 SNCM12169 SNCM12170 SNCM12171 SNCM12172 SNCM12173 SNCM13174 SNCH12175 SNCM13176 SNCM12177 SNCH12178 SNOS12179

SNDT12198 SNCM121SS SNCM12200 SNCH12301 SNOH12202 SNDB12203

SNDT1221S SNCM12216 SNCM122n SNCM1221S SNCH12219 SHCM12220 SNCM12221 SNCH12222 5ND812223

SNDT1222S SNCM12230

SNDT12269 SNCM12270 SNCM12371 SNCM13372 SNOM12273 SNCH13374 SNCM1337S 5NCM12276 SND812277

SNDT12307 SNCH12308 SNCM12309 SNCM12310 SNCM12311 SNDB12312

SNDT13372 SNCH13373 SNCH13379 5NCH133B0 SNOH12391 SNDB12382

DEPTOP

112.940 113.040 114.350 115.420 115.300 116.900 117.590 117.750 118.850 119.700 120.960 132.030 133.360 124.730 136.070 126.140

96.050 56.190 97.450 99.640 95.820

100.940 102.240

41.600 41.700 45.790 45.870

27.140 27.240 28.450 29.610 23.310 31.360 32.120 32.310 33.770 34.920 35.820 36.850 36.960 37.180

91.290 91.500 92.300 93.260 94.230 94.900 95.450 96.390 97.250

125.930 126.040 126.230 126.360 127.000 127.910 128.750 129.340 130.500 131.380 131.480 132.500 133.360

76.180 76.280 77.290 77.380 73.150 79.100 80.180 80.260 81.380 B2.120

53.610 53.730 S4.840 S5.S00 56.760 57.700 58.850 60.100 61.170

129.600 125.700 130.720 130.840 131.360 131.640 132.650 133.650 134.600 135.520 135.640 136.650 137.830 139.020 140.000 140.630 140.910

135.720 135.820 136.860 138.010 138.640 139.040

112.530 112.630 113.680 114.530 116.230 117.150 118.200 118.270 120.010

86.180 86.540

166.030 166.320 167.210 168.500 169.400 170.630 171.790 172.680 173.250

60.640 60.740 61.480 62.200 62.470 63.380

109.690 109.730 116.040 116.320 117.360 115.310

DEPBOT

113.040 114.350 115.420 115.900 116.800 117.590 117.750 113.850 115.700 120.560 122.020 123.360 124.720 126.070 136.140 136.440

96.190 97.450 98.640 99.830

100.940 103.240 102.340

41.700 12.780 15.870 15.970

27.240 29.450 29.610 29.910 31.360 32.120 32.310 33.770 34.810 35.820 36.850 36.960 37.180 37.280

91.500 92.300 93.260 54.230 94.900 95.450 96.390 97.2S0 97.350

126.040 126.230 126.360 127.000 127.910 129.750 129.340 130.500 130.600 131.480 132.500 133.360 133.460

76.280 77.290 77.380 78.150 79.100 80.180 80.260 31.380 82.120 82.220

53.730 54.840 55.900 56.760 57.700 58.850 60.100 61.170 61.270

128.700 130.720 130.840 131.360 131.640 132.650 133.650 134.600 135.520 135.640 136.650 137.830 139.020 140.000 140.630 140.310 140.910

135.820 136.860 138.010 138.640 139.040 139.190

112.630 113.690 114.930 116.230 117.150 118.200 119.270 120.010 120.110

86.540 87.700

166.320 167.210 168.500 169.400 170.630 171.790 172.680 173.250 173.350

60.740 61.480 62.200 62.470 63.380 63.480

109.730 110.330 116.930 117.960 119.310 119.410

RD

2.11 1.33 1.31 2.12 1.31 1.29 1.23 1.31 1.28 1.34 1.29 1.30 1.30 1.29 2.61 1.41

2.33 1.32 1.33 1.35 1.37 1.32 2.43

2.37 1.33 1.91 2.60

2.35 1.30 1.30 1.84 1.33 1.33 1.53 1.31 1.31 1.30 1.31 2.54 1.65 2.64

1.47 1.25 1.28 1.29 1.27 1.31 1.31 1.31 2.24

1.84 1.36 2.02 1.30 1.31 1.31 1.33 1.30 2.67 2.63 1.31 1.32 2.65

1.71 1.30 1.57 1.29 1.28 1.29 1.S8 1.29 1.32 1.78

1.56 1.28 1.28 1.28 1.28 1.27 1.28 1.27 2.47

1.96 1.29 1.78 1.33 1.85 1.29 1.28 1.28 1.27 1.82 1.28 1.27 1.27 1.27 1.28 1.35 2.46

2.30 1.31 1.29 1.31 1.62 2.09

2.34 1.28 1.29 1.28 1.32 1.28 1.27 1.30 2.44

2.12 1.30

2.53 1.34 1.31 1.30 1.32 1.34 1.29 1.30 2.47

2.16 1.36 1.32 1.49 1.34 2.51

1.90 1.33 1.39 1.31 1.29 2.50

ASH

68.00 2.40 1.50

67.80 1.10 1.40 29.70 4.40 .70

2.40 .40 .20

2.10 1.00 90.80 16.50

76.40 1.30 3.30 4.90 7.30 2.90 B4.30

69.32 3.60

49.50 86.50

74.10 1.40 1.40 47.60 1.50 .80

17.00 1.20 .40 .60

1.60 86.10 38.40 88.80

19.80 1.60 .30 .50 .30

1.70 2.10 1.80

70.90

50.30 9.60 61.20 4.60 2.80 2.30 3.30 1.40 89.70 87.10 2.20 6.70

89.20

36.90 1.50 30.40 1.10 .40 .80

31.40 1.10 .80

44.50

25.10 1.80 .70

1.40 .80 .50 .50

1.10 88.40

48.90 1.80 48.70 7.70 57.50 1.60 .40

3.40 .50

28.00 .30 .40 .50 .50

4.00 10.00 86.80

BO.50 5.60 1.10 1.80 37.60 68.60

82.20 1.50 2.80 1.20 3.70 .40 .60

5.20 85.50

66.10 1.30

87.00 S.OO 1.40 .50

1.80 2.10 .80

2.60 35.00

68.60 3.00 1.40

19.90 5.60 84.10

54.50 3.40 .20 .40 .90

85.70

MOIS VM CV 5ULPHIJB

3.10 -5.60 -5.50 -4.00 -6.00 -S.80 -2.70 -5.80 -5.40 -6.03 -5.50 -6.10 -5.60 -5.40 -1.90 -5.50 -

3.20 -6.10 -5.90 -S.20 -6.10 -5.90 -2.40 -

3.20 -5.40 -3.60 -2.50 -

3.30 -5.20 -5.90 -5.30 -6.30 -5.80 -4.60 -6.00 -6.20 -6.00 -5.30 -2.50 -3.90 -2.50 -

3.60 -4.10 -4.90 -6.00 -5.50 -5.10 -4.80 -5.10 -3.90 -

4.20 -4.30 -4.40 -3.80 -4.40 -5.20 -5.00 -5.00 -2.00 -1.60 -6.00 -4.40 -2.10 -

2.90 -4.10 -3.90 -4.90 -S.30 -4.50 -4.SO -4.60 -4.80 -4.00 -

3.20 -3.90 -S.30 -5.10 -5.20 -5.50 -5.40 -4.90 -2.10 -

2.60 -4.30 -4.50 -4.50 -4.10 -S.30 -5.50 -4.90 -5.20 -2.50 -5.90 -5.90 -5.90 -4.50 -1.00 -4.30 -2.20 -

2.70 -1.30 -1.70 -4.50 -3.60 -2.90 -

2.80 -4.20 -3.90 -4.30 -4.30 -4.30 -3.80 -3.50 -3.10 -

3.80 -S.20 -

3.20 -4.40 -5.00 -5.00 -5.00 -5.00 -4.80 • 4.40 -2.50 -

3.00 -S.60 -4.60 -1.20 -1.50 -1.10 -

3.70 -5.00 -5.60 -S.50 -5.00 -2.30 -

1.86 1.80 1.50 .14

1.26 .89 .26 .41 .20 .20 .15 .20 .17 .19 .11 .34

3.62 .40 .30 .15 .30 .20 .14

7.01 1.46 .21 .15

3.18 1.13 .24

1.05 .34 .18 .16 .15 .20 .18 .16 .27 .19 .22

3.49 2.38 1.88 .99 .98

1.15 .72 .72 .32

.25

.26

.27

.19

.17

.16

.19

.21

.20

.70

.33

.40

.22

5.67 2.05 .36

1.23 .66 .74 .49 .27 .24 .85

4.14 2.61 1.5S .97 .33 .69 .55 .67 .28

7.29 2.70 1.75 2.24 1.06 1.29 .53 .35 .22 .04 .19 .18 .19 .20 .23 .22 .46

.31

.29

.20

.25

.29

.30

.08

.33

.20

.15

.15

.15

.14

.19

.05

1.23 .61

.14

.36

.18

.15

.16

.15

.22

.26

.19

.18

.19

.17

.21

.20

.12

.23

.27

.23

.24

.31

.28

Appendix 6.7(confd)

DON

C3038 C3038 C3038 C3038 C3036 C3038 C3038 C3038 C3038 C3039

C3039 C3039 C3039 C3039 C3033 C3039 C3039 C3039

C3040 C3040 C3040 C3040 C3040 C3040 C3040 C3040 C3040 C3040

C3041 C3041 C3041 C3041 C3041 C3041

C3042 C3042 C3042 C3042 C3042 C3042 C3042

C3081 C3081 C3081 C3091 C3081 C3081 C3081 C3081 C3081

C3141 C3141 C3141 C3141

C3143 C3143 03143 03143 03143 C3143 03143 C3143

C314S C3145 C3145 0314S C3145 C314S 0314S C3145 C3145

C3147 C3147 C3147 C3147 03147 03147 C3147 C3147

C3150 O3150 C3150 C31S0 C3150 C3150 C31S0 C3150 C31S0 C3150

C3151 C3151 C3151 C31S1 C3151 C3151 C3151 C3151 C3151 C3151 C3151

C3152 C3152 C3152 03152 C3152 C3152

C3153 C3153 C3153 C31S3 C3153 C3153 C3153 C3153 C3153

C3154 C31S4 C3154 C11S4 03154 C3154 C31S4 C3154 C3154 C3154 C31S4 C31S4 C3154

C31S6 C3156 C3156 C3156 C3156 C3156 C3156 03156

EASTING

37391.71 97391.71 97391.71 97391.71 97391.71 97391.71 97391.71 97391.71 97351.71 57391.71

97191.80 97181.80 97181.80 97181.80 97191.80 97181.80 57181.80 57181.80

97464.09 97464.08 97464.09 97464.08 97464.08 97464.08 97464.08 97464.09 97464.08 97464.09

97513.03 97513.03 97513.03 97513.03 97513.03 97513.03

57063.44 57063.44 37063.44 97063.44 97063.44 97063.44 57063.44

98327.73 99327.73 98327.73 58327.73 58327.73 98327.73 99327.73 98327.73 98327.73

98930.95 98930.95 98930.95 98930.95

98794.71 98794.71 98754.71 98794.71 98794.71 98794.71 98794.71 98794.71

99509.85 98509.85 99509.85 98509.85 98503.85 98509.95 58508.85 98509.95 98509.95

98603.07 98603.07 98603.07 98603.07 99603.07 99603.07 98603.07 98603.07

98661.34 93661.34 88661.34 98661.34 88661.34 98661.34 99661.34 98661.34 98661.34 98661.34

98938.15 98838.15 98838.15 98838.15 98839.15 98838.15 99938.35 99938.15 99938.15 98838.15 99838.15

98607.12 99607.12 98607.12 98607.12 98607.32 99607.12

98714.75 98714.75 93714.75 98711.75 98714.75 99714.75 98714.75 98714.75 98714.75

98371.54 98371.54 98371.54 96371.54 98371.54 98371.54 96371.54 98371.54 98371.54 58371.54 98371.54 98371.54 98371.54

99382.61 98382.61 98383.61 98383.61 98383.61 98383.61 99363.61 98383.61

NORTHING

194873.55 194879.55 194879.55 134873.55 134679.55 194879.55 194873.55 134979.55 134873.55 194879.55

195137.03 135137.03 195127.02 195127.03 195127.03 195137.02 155137.03 155127.02

195498.22 195458.22 195438.22 135498.22 195498.22 195498.23 195498.33 195499.33 195438.33 135438.23

195746.91 195746.91 195746.31 195746.91 195746.51 195746.91

155746.11 155746.11 195746.11 135746.11 155746.11 155746.11 155746.11

154756.35 134756.35 134756.35 134756.95 194756.95 194756.95 194756.95 194756.95 194756.35

135250.02 135250.02 135250.02 135250.02

135004.84 195004.84 135004.84 135004.84 135004.84 135004.84 135004.84 155004.84

155120.03 155130.03 195130.03 195120.03 195130.03 195130.03 195130.03 195120.03 195120.03

195130.44 195130.44 195130.44 195130.44 155130.44 155130.44 155130.44 155130.44

155258.56 155256.56 155258.56 155258.56 195359.56 195359.56 195358.56 195258.56 195358.56 195358.56

195377.23 195377.23 135377.23 195377.23 195377.23 195377.23 195377.33 195377.23 195377.23 195377.23 135377.23

195378.94 195378.94 195378.54 135378.94 135378.54 135378.34

135503.20 195503.20 135503.20 155503.20 135503.20 155503.20 155503.20 155503.20 155503.20

135388.59 195388.59 195388.59 195388.59 195388.59 195398.59 195388.58 195388.59 195398.59 195388.59 195388.53 195388.59 19S398.59

195504.95 195504.95 195504.95 195504.95 135504.95 195504.95 195504.55 155504.35

SAMP. NO.

SNDT12331 SNCM12333 SNCM13333 SNCM13394 SNCM13395 SNCM13396 SNCM13337 SNCM133S8 SNDB13399 SNDB12400

SNDT12S34 SNCH12S2S SNCM12526 SNCM12537 SNCH13539 SNCM13529 SNCM12530 SNCM12531

SNDT12463 SNCM13464 SNCM13465 SNCM12466 SNCM13467 SNCM12468 SNCM12469 SNCH12470 SNOB12471 SNDB12473

SNDT12494 SNCM1349S SNCM13496 SNCM12497 SNCM13498 SNDB13439

SNDT13512 SNCH13513 SNCH1251! SNCM12515 SNCM12516 SNCM12S17 SNDB12518

SNDT12683 SNCM12684 SNCM12685 SHOM12686 SNCM12687 8NCM12688 SNCM126BS SNCM12630 SNDB13631

SNCM12763 SNCM12770 SNCM12771 SNCM12772

SNDT12773 SNCM12774 SNCM12775 SNCM13776 SNCM12777 SNCM12778 SNCM1277S SNDB13780

SNDT13781 SNCM127 8 2 SNCM127 83 SNCM12784 SNCM127 85 SNCM12786 SNCM127 87 SNCM127 88 SNDB12789

SNDT127 30 SNCM127 91 SNCM13792 SNCM127 33 SNCH137S1 SNCM137 35 SNCH12796 SNDB137 37

SNDT12831 SNDT12833 SNDT13833 SNDT13831 SNCM1283S 5NCM138 36 SNCM13837 SNCM12838 SNCM12838 SNDB12840

SNDT12S46 SNDT12847 SNDT12848 SNDT12845 SNCM128S0 SNCM12851 SNCM12852 SNCM12853 SNCM12854 SNCM12855 SNDB12856

SNDT128S7 SNCM12858 SNOM12859 SNCM12860 SNCM12861 SNDB12862

SN 12888 SN 12889 SN 12990 SN 12891 SN 12892 SN 12893 SN 12894 SN 12895 SN 12896

SNDT12863 SNDT12864 SNDT12865 SNCM12866 SNCM12867 SNCM12868 SNCM12S69 SNCM12870 SNCM13872 SNDB12872 SNDB12873 SHDB12874 SNDB12875

SNDT12876 SNDT12877 SNDT12878 SNCH12879 SKM12830 SNCM12881 SNCM12883 SNCH13883

DEPTOP

62 63 64 66 67 68 69 70 70 71

52 52 53 54 55 56 57 59

125 125 127 127 128 129 130 131 132 133

138 138 139 140 141 143

98 98 99

100 101 103 104

37 37 38 29 30 31 32 33 34

29 30 31 32

29 29 29 30 32 33 34 35

28 28 28 29 30 32 33 34 35

28 28 28 30 31 33 34 35

47 47 48 46 48 49 51 52 53 53

39 39 39 40 40 41 42 13 14 16 17

49 19 49 SO 50 SI

11 11 12 42 13 11 14 14 46

47 48 48 48 19 50 SI SI 52 51 54 54 55

37 38 38 38 39 41 42 43

960 870 950 060 060 070 070 120 680 200

620 720 300 260 600 140 570 480

760 860 000 150 260 150 160 320 570 870

050 ISO 280 660 670 250

640 7 40

730 820 950 380 100

780 880 230 420 830 370 210 140 270

570 230 320 370

410 SOO 670 870 070 270 470 490

570 670 860 360 960 040 160 360 440

190 320 520 730 930 130 130 020

620 7 20

030 220 570 550 190 240 100 990

050 170 640 000 350 100 920 880 850 020 140

110 210 750 460 610 610

640 840 480 700 530 040 S60 580 080

900 000 670 860 860 030 140 900 950 000 400 560 220

930 030 510 710 970 060 540 7 30

DEPBOT

63 64 66 67 68 69 70 70 71 71

52 53 54 55 56 57 59 58

125 127 127 128 129 130 131 132 132 132

138 139 140 141 142 142

98 99

100 101 103 104 104

27 29 25 30 31 32 33 34 34

30 31 32 33

25 25 30 32 33 34 35 35

28 28 29 30 32 33 34 35 35

28 29 30 31 33 34 35 35

47 49 48 48 49 SI 52 S3 S3 54

39 39 40 40 41 43 43 44 46 47 47

49 49 50 50 51 SI

41 43 43 43 14 44 44 46 46

49 48 18 49 50 51 SI S3 54 54 54 55 55

38 38 38 39 41 42 43 45

870 950 060 060 070 070 130 680 300 300

730 300 360 600 140 570 480 730

860 000 ISO 260 190 160 320 570 870 970

150 280 660 670 250 350

7 40

790 820 950 390 100 210

880 230 420 330 370 210 140 270 370

230 320 370 850

500 670 870 070 270 470 490 590

670 860 860 960 040 160 360 440 540

320 520 730 530 130 130 020 150

720 030 220 570 950 190 240 100 990 090

170 640 000 350 100 820 880 850 020 140 240

210 750 460 610 610 770

840 480 700 530 040 560 980 080 200

000 670 860 660 030 140 900 850 000 400 S60 220 330

030 510 710 870 060 540 7 30

110

RD

2.03

1.31

1.38

1.30

1.39

1.39

1.36

1.30

1.44

2.62

2.21

1.35

1.30

1.30

1.29

1.30

1.29

1.45

2.90

1.31

1.32

1.31

1.32

1.30

1.30

1.29

1.41

2.19

2.52

1.32

1.33

1.30

1.33

2.39

3.52

1.31

1.30

1.32

1.31

1.32

2.51

2.05

1.30

1.43

1.30

1.30

1.29 1.30

1.30

2.37

1.81

1.69

1.64

1.68

2.58 1.58

1.31

1.31

1.31

1.29

1.27

2.35

2.40

1.52

1.3S

1.30

1.33

1.30

1.39

1.28

2.29

2.52

1.31

1.32

1.30

1.31

1.23 1.28

2.53

1.90

1.33

2.30

1.39

1.30

1.28

1.25

1.27

1.29

2.49

3.30

1.31

3.49 1.39

1.30

1.39 1.25

1.29

1.29

1.29 2.36

2.43

1.45 1.37

1.51 1.30

1.69

1.90

1.33

1.35

1.33

1.30

1.31

1.33

1.40

2.55

2.61

1.36

2.45 1.36

1.67

1.30

1.29

1.30

1.27 1.48

3.12

1.31

3.63

3.44

1.40

2.39

1.34

1.23 1.29

1.31

1.33

ASH

63 1 1

1 2 17 89

61 6

1 18

63 1 5 1 1

1

15 71

84 3 3 1 4 80

79 2

3 83

59 1 18 1

2 77

1 1 1 2

83 30 1

75

79 2S 7

1 73

85

1

1

2 B0

56 6

74 12 1

6 65

74 4 B2 12 2

3 76

79 23 1 26 2 45

59 2 4 1

2 9 19 89

68 B 82 9 37 2

1

21 68 5 88

Bl 15 61 S

1 6

20 10 20 70 60 40 30 30 SO 50

90 80 80 SO 40 50 80 20

70 30 30 60 90 60 60 50 10 40

80 30 10 40 30 60

SO 60 70 90 30 90 50

SO 30 80 00 76 33 SO 30 20

50 07 31 90

50 20 00 71 SI 70 65 00

50 70 50 87 38 30 42 60 80

73 92 22 91 09 66 50 96

60 80 90 65 68 45 47 72 65 35

76 07 37 96 06 66 24 30 36 17 67

03 OS 20 40 12 12

38 91 48 67 46 81 07 77 25

00 SO 40 S3 57 55 80 87 66 63 78 08 20

96 50 00 03 27 67 SO 84

MOIS VM

3.60 -

5.10 -

4.70 -

5.50 -

5.00 -

5.30 -

5.00 -

4.40 -

3.90 -

3.00 -

3.60 -

5.00 -

5.60 -

6.00 -

6.20 -

5.70 -

4.70 -

4.90 -

3.30 -

5.10 -

1.60 -

5.00 -

5.10 -

5.40 -

4.80 -

4.40 -

4.50 -

3.20 -

3.10 -

4.30 -

5.30 -

4.50 -

5.40 -

2.50 -

3.60 -

5.30 -

5.90 -

5.50 -

5.60 -

5.50 -

3.60 -

3.07 -

4.50 -

3.60 -

4.80 -

5.20 -

4.80 -

4.90 -

4.10 -

3.60 -

18.02 -

15.58 -

16,.05 -

13.06 -

2.36 -

3.61 -

4.90 -

4.76 -

4.82 -

4.29 -

1.93 -2.17 -

3.35 -

3.55 -4.50 -

4.80 -

S.03 -

4.80 -

4.60 -

4.00 -

1.13 -

2.17 -

1.64 •

4.93 -

4.91 -

4.62 -

4.51 -

4.01 -

4.06 -

3.95 -

4.05 -

4.37 -

4.41 -

4.96 -4.90 -

4.77 -

4.35 -

3.67 -

2.47 -

3.83 -

4.85 -

3.85 -

3.96 -4.86 -

S.OO -5.17 -

S.46 -

S.18 -

3.95 -4.03 -

3.33 -

1.14 -1.64 -

1.35 -

1.66 -

3.73 -

3.65 -

5.27 -

5.35 -

5.35 -

5.56 -

1.77 -

1.27 -

3.53 -

2.25 -

2.21 -

1.60 -

3.72 -4.33 -

4.18 -5.28 -

4.SO -

5.00 -

5.25 -

4.32 -

3.60 -

1.11 -

1.14 -

3.87 -

4.30 -

1.78 -

1.99 -

5.18 -

5.22 -

1.80 -

1.19 -

OV SULPHUR

.13

.10

.21

.15

1.50

.67

.24

.16

.16

.15

.16

.32

.13

.28

.18

.16

.20

.16

.15

.14

.21

.21

.18

3.84

1.43 .38

.22

.17

.16

.10

3.40

.44

.30

.30

.16

.19

.16

.20

.32

.33

.30

.13

.40

.34

.30

.30

.18

.30

.17

.57

.13

.33

.21

.36

.16

.17

.20

.56

.30

.47

.50

.26

.26

.34

.23

.37

.20

.32

.20

.23

.63

.34

.25

.22

.22

.IS

.15

.15

.25

.20

.31

.11

.23

.30

.15

.15

DDH EASTING NORTHINO SAMP. No. DEPTOP DEPBOT RD ASH MOIS VM CV

C3156 99382.61

03156 98382.61

C3156 99383.61

C3157 98364.93

C3157 98364.93

03157 96364.53

C31S7 59364.93

C3157 98364.53

195504.95 SNDB13984

195504.95 SNDB13985

195504.95 SNDB12886

195259.38 SNDT13910

155358.38 SNDT13911

195358.38 SNCM13913

135258.38 SNCM12913 195259.38 SNDB13914

C31S9

C3159

C3159

C3159

C3159

C3159

C3159

03159

03159

03159

99030.05

99030.05

99030.05

99030.05

99030.05

99030.05

93020.05

99030.05

99020.05

99020.05

195070.98

195070.98

195070.39

135070.90

195070.99

195070.99

195070.98

195070.98

135070.38

195070.99

SHDT12893

SNDT12300

SNDT13501

SNCM12303

SNOM13903

SNCM12904

SNCM13905

SNCH12906

SNOM12307

SNDB13308

O3330 98911.34

C3330 98811.34

C3230 38811.34

C3230 38811.34

C3230 98811.34

O3230 99811.34

O3330 98811.34

C3331

03331

03331

C3331

C3331

C3331

C3231

C3231

C3331

03231

C3231

C3231

03231

C3231

C3233

C3233

C3233

03233

03233

03233

03233

03233

C3233

03233

C3233

C3234

03234

03234

03234 C3234

C3234

03234

03234

03236 C3236

03236

C3236

03236

C3236

03236

C3236

C3236 03236

03236

C3236

03236

03236

C3237

03237

C3237

C3237

C3237

C3237

C3337

C3237 C3237

C3237

03368 C3368

03368

C3368

C3368

C3368

C3368

C3369

C3369

C3369 C3369

C3369 C3369

03369

C33S1

C33S1

C3331

C3391

C3391

C33S1

C3331

C3391

C3391

C3392 C3392

C3392

C3392

C3332

C3332

03332

03352

C3332

C3393

C3333

C3333

C3333

C33S3

C33S3

C33S3

C3393

03353

C3355

C33SS

C3395

C33S5

C335S

C3395

C339S

C3395

C3396

C3396

C3396

03396 C3336

58758.27

58758.27

98758.27

98756.27

98756.27

96758.27

59753.27 58758.27

99758.27

98758.27

99758.27

99758.27

99758.27

98758.27

98906.30

98906.30 98506.30

58806.30

99806.30

38306.30

96306.30

99906.30

98906.30

98906.30

98906.30

98752.25

98752.25

98752.35

987 53.35 98753.35

98753.35

98753.25

98752.25

99823.58

98823.58

58823.58

98823.58

98823.58

98623.58

98823.58 98823.58

98923.58 88823.58

38823.58

98823.58

98823.58 99923.58

98759.49

98759.49

99759.49

98759.49

98759.45

96759.49

987S9.49

98758.49

99759.49

96759.45

100035.38

100035.38

100035.38

100035.38

100035.38

100035.38

100035.38

100013.55

100012.55

100012.55

100012.55

100012.55

100012.55

100012.55

59187.70

33187.70

99187.70

95187.70

55187.70

99197.70

99187.70

93187.70

35187.70

55215.15

99215.15

99215.15

99215.15

99215.IS 33215.IS

53215.15

99215.15

53315.15

99334.58

35354.58

85234.58

85254.58

99354.58 96394.59

99394.58

99394.58

99394.58

99365.07

99365.07

99265.07

99365.07

99365.07

99365.07

99365.07

99365.07

33131.79

35131.79

99131.79

99131.79

99131.79

135191

195181

195181

L9S18I

195181

195191

195181

195447 195447

195447

195447

195447

155447

155447

155447

135447

135147

195447

195447

195447

195447

59 SNDT13039

.59 SNCM13040

.59 SNCM13041

.59 SNCM13042

59 SNCH13043

59 SNCM13044

59 SNCM13165

.36 SNDT13045

.16 SNCM13046

16 SNCM13047

.16 SNCH13048

16 SNCM13049

.16 SNCM13050

16 SNCM13051

16 SNCH13052

16 SNCM13053

16 SNCM13054

16 SNCM13055

16 SNDB33056

16 SNDB13057

16 SNDB13059

195454.05

155454.09

195454.09

195454.09

195454.09

195454.09

195454.09

195454.09

195454.09

195454.09

195454.09

SNDT13068

SNDT13069

SHCM13070

SNCM13071

SNCM13072

SNCM13073

SNCM13074

SNCM13075

SNOH13076

SNCH13077

SND813078

45.110

45.460

45.930

11.740

11.840

12.430

13.390

16.080

23.010

22.130

22.930

23.540

24.340

2S.300

36.300

27.310

38.410

28.330

38.650

36.750

28.750

30.100

31.100

31.630

31.730

38.240

38.340

38.740

35.130

35.470

33.540

40.930

41.660

13.310

13.110

44.500

44.900

46.000

45.260

18.080

48.180

48.860

43.660

50.490

51.500

52.500

54.050

54.260

55.400

55.600

45.460

45.930

46.060

11.940

12.430

13.390

15.080

15.180

23.130

33.920

23.540

24.340

25.300

36.200

37.310

38.410

39.330

39.900

38.750

29.750

30.100

31.100

31.630

31.730

31.910

38.340 38.740

39.130

39.470

39.940

40.930

41.660

43.210

43.410

44.500

14.900

45.000

45.360

45.360

49.180

48.860

19.660

50.190

51.500

52.500

54.050

54.260

55.400

55.600

55.700

1.63 3.90

1.86 53.80

2.36 78.78

3.31 -

3.14 -

3.97 -

3.54 85.11 3.13

1.72 41.34

1.32 3.63

1.31 1.33

2.51 86.27

4.04 -

5.40 -

5.06 -

2.31 -

1.33 2.50

1.32 3.00

.33 12.60

.31 1.30

.37

.21

.82

.42

.52

2.03 60.77

1.30

1.28

1.31

1.30

2.35 72.50

1.33 1.35

1.33 .80

1.31 .60

1.33 2.00

2.26 74.50

2.30 71.90

1.99 61.23

1.32 4.86

3.39 79.44

1.37 13.17

1.35 5.55

1.33

1.31

1.39

1.30

1.31

1.33

.34

.54

.46

1.22

1.41

5.

2.63 95.15

1.46 23.69

2.62 90.05

1.73 44.10

1.34 6.90

1.31 .80

1.31 .40

1.30 .86

.63 87.90

.35 9.70

56 29. 80

5.15

4.50

4.65

5.25

5.38

5.13

5.30

4.77

4.32

3.02

3.03

4.50

4.30 .

4.30 .

4.20 .

2.30 .

2.40 .

3.07 •

3.97 •

3.20 -

4.00 .

3.99 -

4.56 •

4.67 -

4.80 -

4.52 -

4.15 -

3.32 -

3.IS -

2.91 -

2.09 -

1.42 -

4.20 -

4.36 -

S.02 -

1.36 -

1.73 -

1.37 -

2.44 -

3.40 -

3.12 -2.80 -

185065.86 SNDT1307S 7.110 7.210 2.56 86.93 2.79

195065.86 SNCM1308

195065.86 SNCM13081

195065.86 SNOM13083

136065.86 SNCM13083

195065.86 SNCM13084

7.210

7.890

8.990

10.ISO

11.300

990

8.330

10.150

11.300

11.370

1.31

1.29

1.29

1.31

1.32

.20

.55

1.09

2.57

5.32

1.38

1.56

1.61

1.73

195065.86 SNCM13095 11.970 13.470 1.32 2.99 4.21

195065.86 SNDB13086 12.470 12.570 2.54 86.78 2.55

195301. 155301

155301

195301.

135301.

135301.

195301

195301.

195301.

155301.

155301.

195301.

195301.

155301.

41 SNDT13092

11 SNDT13093

11 SNDT13091

41 SNDT13095

41 SNDT13036

41 SNCM130S7

41 SNCM130S9

41 SNCM13033

41 SNCM13100

41 SNCM13101

41 SNOM13102

41 SNDB13103

41 SNDB13104

41 SNDB13105

135066.34

135066.84

135066.84

195066.84

195066.94

195066.94

195066.94

195066.84 195066.91

195066.91

203808.63

203806.63

203808.63

203808.63

203808.63

203808.63

203808.63

201475.77

204475.77

204475.77

204475.77

204475.77 204475.77

204475.77

202491.70

202491.70

202491.70

202491.70

202491.70 202491.70

202491.70

202491.70

202491.70

202249.99

202249.98

203349.99 202249.98

202249.98

202249.98

202249.98

203349.98

303349.98

302020.34

202020.34

203030.34

303030.34

203020.34

202020.34

202020.34

202030.34

202020.34

201483.06

201483.06

201483.06

201483.06

201483.06

201483.06

201483.06

201483.06

201020.63

201020.63

201020.63

201020.63

201020.63

SNDT13106

SNDT13107

SNDT13108

SNCM13109

SNCM13110

SNCM13111

SNCH13112

SNCM13113

SNCM13114

SNDB13115

SN 13385

13366

13387

13388

13389

13390

13391

13356

13357

13358

13359

13360

13361

13362

13473

13474

13475

13476

13477

13478

13479

13480

13481

13495

13496

13497 13498

13499

13500

13S01

13502

13503

13522

13523

13524

1353S

13536 13537

13539

13539

13530

47.520

47.620

48.030

48.200

49.040

49.210

49.450

15.550

50.220

53.380

54.490

55.430

55.620

56.010

7.790

7.990

B.780

9.010

9.750

10.560

11.000

11.930

12.680

13.080

73.400

73.SOO

73.500 73.950

74.550

75.550

77.170

28.450

28.550

28.700 29.700

30.700

31.700

32.060

91.910

92.010

93.600

93.600

94.600

94.700

96.310

97.470

98.480

104.300

104.400

105.400

106.400

107.400 108.400

109.190

109.800

110.620

82.190

82.290

92.130

83.500

84.820

35.800

87.300

88.000

88.540

13554 135.790

13555 135.850

13556 136.800

13S57 138.450

13558 140.220

13559 140.640

13560 141.450

13561 142.700

13563

13564

13S6S

13566 13567

58.500

58.600 58.500

60.500 61.900

47.620

48.030

48.200

49.040

49.210 19.450

19.550

50.220

53.380

51.150

55.130

55.620

56.010

56.110

7.850

9.780

9.010

9.750

10.560

11.000

11.930

12.680 13.080

13.180

72.500

73.500

73.950

74.950

75.950

77.170

77.270

28.550

38.700

39.700

30.700

31.700

33.060

33.160

53.010

52.600

63.600

94.600

95.700

96.310

97.470

98.480

58.580

104.400

105.400

106.400

107.400

108.400

108.150

109.800

110.620

110.730

82.290

82.430

63.500

84.820

85.800

67.300

88.000

88.540

88.640

135.890

136.800

138.450

140.220

140.640

141.450

142.700

143.380

58.600

55.900 60.900

61.900 62.900

2.38 80.70

1.33 5.20

1.82 50.10

1.31 3.20

2.21 71.20

1.34 8.20

1.44 20.10

1.30 2.90

1.31 .60 1.31 .80

1.27 .60

1.83 51.10

1.31 6.40

2.38 83.20

2.80

4.60

3.30 3.50

1.20

3.80

3.20

3.30

.53 83.20 2.22

.32 1.70

.17 73.70

.34 2.70

31

1.32

2.50

1.05

1.30 1.50

1.31 2.10 1.40

1.23 1.00

1.31 1.00 1.30 1.70

2.56 68.00

1.30

1.30 1.50

2.30

1.62 23.33 5.34 -

1.35 1.40 3.10 -

2.13

.85 .80

.11 .33 1.15 9.67

.04 59.02 5.69

24 67.86

55 19.37

34 2.33

1.32 2.19

1.34

1.33

1.32

1.32

1.34

1.33

1.32

3.65

6.17

7.95

9.06

9.76

9.95

1.81

1.43 7.86

.51 7.32

1.53 6.68

1.87 50.38 5.64

2.15 68.61

1.33 1.10

1.32

1.31 .67

.23

.28

2.21 69.63

1.42 5.87

1.34 .60

1.33

1.31

1.33

1.32

1.30

.23

.25

.13

2.38 76.72

1.33 1.05

1.33 1.22

11 .65

12 12.23

13 .39

31 .59

84 49.30

4.34

S.75

6.32

6.17

7.94 7.50

7.87

7.06

5.87

5.06

5.79

6.73

6.68

7.39 7.62

7.02

5.96

5.30

4.74

6.99

7.10

7.SO

6.87

7.58

7.43 6.16

1.78 41.89

1.33 2.46 1.31

1.31 .43 1.31 .56 7.36

5.09

.12

7.72

7.4]

.17

.17

.20

.05

.23

.21

.19

.20

.30

1.96

1.24

.86

.40

.27

.52

.36

.22

.34

3.30

.46

.26

.28

.27

.28

.21

.12

.34

.28

.18

.19

.20

.21

.21

.19

.19

.23

.31

.21

.19

.37

.17

.16

.20

.18

.20

.21

.22

.31

.33

.26

.19

.31

.50

.28

.53

.30

.25

.41

.21

.26

.21

.34

3.36

1.32

.45

.24

.17

.27

.43

3.79

4.70

.19

3.23

2.38

1.95

.99

.33

.30

.26

.34

.73

1.53

2. S3

1.4S

.49

.32

.32

.36

.43

.56

.34

.27

.29

.33

1.48

2.39

.90

.30

.93

.53

.37

.57

3.52

.75

.25

.32

.45

Appendix 6.7 (confd)

DDH EASTING

C3396 93131.79

C3396 99131.79

C3396 99131.79

C3396 93131.79

C3397 99168.54 C3397 99168.54

C3397 96166.54

C3397 99168.54

C3397 99168.54

C3397 99168.54

C3397 99168.54

C3397 99169.54

C3397 93168.54

C3397 99168.54

C2397 99168.54

C3393 98644.70

C3399 98644.70

03399 98644.70 03399 38644.70

C3399 98644.70

C333S 58644.70

C3399 38644.70

C333S 58644.70

C3399 98644.70

03399 96644.70

C3359 98644.70

C3399 99644.70

C3400 99505.51

C3400 96505.51

03400 33605.51

C3400 33505.51

C3401 97613.91

C3401 97613.91

03401 97613.91

C3401 97613.91

C3401 97613.91

C3409 99004.14

O3409 99004.14

O3409 95004.14

C3405 59004.14

O3409 55004.14

03409 99004.14

C3410 97617.33

03410 97617.33

C3410 97617.33

C3410 97617.33

C3410 97617.33

C3410 97617.33

C3443 59916.22

03443 99916.23

03443 39916.33

C3443 95516.22

C3443 55516.22

C3445 53260.37

C3445 99260.57

C3445 55260.97

03445 99360.97

C3445 99360.97 C3445 99360.97

C3445 95260.97 C3445 95260.97

C3446 98676.00

03446 98676.00

C3446 98676.00

C3446 98676.00

C3482 96494.19 C3482 96454.19

03482 96494.15

C3482 86454.19

C3482 96494.19

03492 96494.19

03482 96494.19

C3484 96632.53

C3484 96632.53

C3484 96632.53

03484 96632.53

03484 96632.53

03484 96632.53

C3484 96633.53

03486 96235.31

C3486 36233.31

C3486 96239.91

03486 96239.91

03486 96339.91

03496 96339.91

03491 96364.23

C3491 96364.22 C3491 96364.22

C3491 36364.22

C3431 56364.23

C3491 96364.22

C3491 96364.22

C3492 96599.69

C3492 96595.69

03492 96599.69

C3492 96599.69

03492 36535.65

C3432 36599.69

C3492 96599.69

03493 96936.06

C3433 96836.06

C3493 96836.06

03493 96936.06

C3493 96836.06

C3493 56836.06 C3493 96836.06

C3493 96836.06

C3493 96636.06

03495 96921.30

C3495 96321.30

C3455 56531.30

C3465 56531.30

C3495 96921.30

C349S 96921.30

C3495 96921.30

C34S5 96921.30

C349S 96321.30

C3435 66531.30

C34S5 36521.30

C31S5 56631.30

C34S6 96848.11

C3196 96948.11

C3496 96848.11 C34S6 66848.11

C3456 96848.11

C3496 96849.11

C3496 96849.11

C3496 96648.13

C3496 96648.11

C3496 96948.11

03496 968 48.11

C3500 36883.57

C3500 36863.57

NORTHING

301020.63

301030.63

301030.63

301020.63

300536.55

300536.55

300536.55

200S26.55

200536.55

200526.55

300536.55

300536.55

300536.55

300536.55

300536.55

300254.37

300354.37

200354.97 300354.37

300354.37

200254.37

200354.97

300354.37

300354.37

300354.37

300354.37

200254.37

303337.34

303337.34

303337.34

303337.34

155137.88

195127.88

195137.88

135137.88

195127.88

135767.42

155767.42

195767.42 195767.42

155767.42

155767.42

135127.55

195127.55

195127.55

195127.55

195127.55

195127.55

203759.03

203759.02

203758.02

203758.03

203758.02

203019.08 303013.08

203019.08 303013.08

303019.08

303019.08

203019.08 203019.08

201463.09

201463.03

201463.03

201463.09

194680.15

184680.15

194680.25 184680.15

134680.15

134680.15

194680.15

134755.00

194755.00

134755.00

154753.00

134753.00

194759.00

194753.00

194822.64

134822.64

194822.64

134822.64

194822.64

194822.64

195123.16

155122.16 155123.16

195122.16

155123.16

195122.16

195122.16

194882.08

184882.08 194882.08

194882.08

194882.08

194982.08

194882.08

194875.43

194875.41

154875.41

154875.41

194875.41

19487 5.41

194875.41

194875.41

194875.41

195039.64

195039.64

135039.64

195035.64

I9S039.64

135039.64

195039.64

195035.64

155038.64

195039.64

195039.64

195035.64

195122.07 155122.07

195122.07 195122.07

195122.07

195133.07

195122.07

195123.07

155133.07

195322.07

155122.07

164751.26

164751.36

SAMP. No.

SN 13568

SN 13569

SN 13570

SN 13571

SN 13573

SN 13573

SN 13574 SN 13575

SN 13576 SN 13577

SN 13578

SN 13579 SN 13580

SN 13581

SN 13582

SN 13599

SN 13600

SN 13601

SN 13603

SN 13603

SN 13604

SN 13605 SN 13606

SN 13607

SN 13609

SN 13609

SN 13610

SN 13634

SN 13625

SN 13626 SN 13627

SNDT13650

SNCM13651

SNCM13653

SNCM13653

SNCM13654

SNDT13657

SNCM13658

SNCM13659 SNCM13660

SNDB13661

SNDB13663

SN 13699

SN 13700

SN 13703

SN 137 03

SN 13704

SN 13705

SN 137 50

SN 13751

SN 13752

SN 13753

SN 13754

SN 13771

SN 13772

SN 13773

5N 13774

SN 13775 SN 13776

SN 13777

SN 13778

SN 13793

SN 13734

SN 137 SS

SN 13796

SNDT13904 SNCM13S0S

SNCM13906 SNCM13907

SNCM13908

SNCM13909

SNDB13310

SNDT13311

SNCM13913

SNCM13913 SNCM13914

SNCM13915

SNCM13316

SNDB13317

SNDT13839 SNCM13319

5NCM13930

SNCM13321

SNCM13S22

SNDB13S23

SNDT13930

SNCM13931

SNCM13933

SNCM13933

SNCM13334

SNCM1333S

SNDB13536

SNDT13940

SNCM13941

SNCH13942

SNCM13343

SNCM13544

SNCM1354S

SNDB13S46

SNCM13950

SNCM13353

SNCM13952

SNCM13953

SNCM13554

SNCM13S5S

SNCM13S56

SNCM139S7

SNDB139S8

SNDT13959

SNCM13960

SNCM13961

SNCM13962 SNCHI3963

SNOM13964

SNCM13965

SNCM13366 SNCM13367

SNDB13568

SNDB13969

SNDB13370

SNDT1397]

SNCM13372

SNCM13S73

SNCM13374

SNOM1337S

SNCM13976

SNCM13S77 SNCM13S79

SNCM13S79

SNCM13380

SNDB13581

SNDT14003

SNCM14004

DEPTOP

63.500

63.600

64.630

64.740

58.350 56.350

59.350

6O.3S0

61.3S0

63.350

63.350

64.350

65.230

65.440

66.460

103.730

103.930

104.830

105.830

106.830 107.830

108.830

109.830

110.830

111.830

112.830

113.550

123.600

123.640

127.870

128.900

136.330

136.410

137.300

138.030

138.600

26.620

27.620

28.630

39.630

30.910

31.300

136.380

137.120

138.500

138.500

140.350

140.470

113.750

112.850

115.140

116.640

117.830

134.740

134.810

135.840 136.840

137.840

138.840

139.840 140.820

133.840

133.940

134.940

135.900

45.920

46.020

46.980

48.400

48.160

50.170

52.210

42.780

12.880

14.380

45.880

17.380

18.110

18.960

19.410

13.510

21.010

22.510

24.010

25.830

60.480

60.580 62.080

63.580

65.080

66.080

67.470

80.610

60.790

82.290

83.750

85.250

86.440

87.540

54.850

55.680

57.170

57.600

57.700

59.200

60.700

61.700

63.910

39.510

39.610

10.650

11.750

41.560

43.400

44.300

46.030

16.130

17.620

18.270

13.020

14.790

45.020

46.160

17.520

18.030

49.530

51.030 52.520

53.590

54.990

56.030

26.240 26.340

DEPBOT

63.600

64.620

64.740

64.940

58.3S0

59.350

60.350

61.350

63.350

63.350

64.350

65.330

65.440

66.460

66.560

103.830

104.830

10S.830

106.830

107.830

108.830

108.630

110.830

111.830

112.830

113.550

113.650

133.640

127.870

138.800

139.940

136.410

137.200

137.930

138.600

140.100

27.620

28.630

39.630 30.650

31.300

31.400

137.130

137.500 139.500

140.350

140.470

140.570

113.650

115.140

116.640

117.830

118.030

134.840 135.840

136.840

137.840

138.840 139.840

140.820

140.920

133.340

134.340

135.300

136.770

46.020

46.380

48.400 43.160

50.170

52.210

52.310

42.860

44.380

45.880

17.380

18.410

43.360

50.060

19.510

31.010

32.510

24.010

25.830

26.040

60.580

62.080 63.580

65.080

66.080

67.470

67.570

80.730

82.290

83.790

35.230

B6.440

87.340

88.040

55.960

57.170

57.600

57.700

59.200

60.700 61.700

62.610

63.010

35.610

40.650 41.750

11.660

42.400

14.200

46.020

46.120

47.620

46.270

43.020

43.130

45.020

46.460

47.520

48.020

43.520

51.020

52.530 53.530

54.850

56.030

56.150

26.340

27.540

RD

1.32

1.33

1.31

2.16

2.37

1.33

1.32

1.31

1.32

1.31

1.31

1.33

2.29

1.33

3.12

2.48

1.33

1.32

1.32

1.23

1.33

1.32

1.26

1.28

1.30

1.30

2.45

1.32

1.31 1.32

1.32

1.62

1.31

1.30

1.41

1.31

1.30

1.31

1.31 1.28

1.35 2.40

2.49

1.41 1.32

1.31

1.98

2.34

1.69

1.34

1.36

1.32

1.59

1.70

1.33

1.33 1.31

1.32

1.32

1.31 1.79

2.52

1.33

1.32

1.33

2.45

1.35

1.32 1.33

1.S5 1.32

2.70

2.05

1.33

1.32

1.33

1.33

1.31

2.38

2.10

1.32

1.30

1.32

1.33

2.44

2.25

1.31

1.31

1.29 1.34

1.30

2.44

1.96

1.31 1.30

1.30

1.32

1.31 2.59

1.30

1.31

2.39

1.95

1.32

1.30 1.28

1.29 2.63

2.60

1.30 1.30

1.57

2.59

1.32

1.33

2.56

1.33

2.73

1.35

2.64

1.95

1.31

1.31 1.30

1.30

1.29

1.29 1.33

1.31

1.29

2.17

2.31

1.33

ASH

.46 3.04

.57 67.62

76.60

1.01

.36

.63

.64

.35

.77 1.03

77.29

1.99

71.03

83.03

.98

.41

.43

.85

.91 1.03

.47

.34

.53 1.91

83.50

.48

.39

.44 1.63

36.75

1.03

1.36

13.16

2.41

.78 1.53

1.46 .68

8.37

78.22

84.70

3.10 2.20

1.80

60.40

78.60

32.24

1.20

4.33

.71 37.87

37.45 .66 .54 .51 .35 .74 .83

46.14

83.66

1.17 .73 .73

73.53

3.31

.80

.50

.37 1.71

65.64

59.49

.94

.93

.23 3.06

1.29

90.43

61.95 1.41

.45

.46 1.60

60.08

70.31

1.08

1.59

.45 4.26

1.25

84.63

53.49

.88 1.22

.20 2.87

.83 68.26

.73 2.57

75.76

49.66

3.19

.97

.73 1.14

39.36

97.12

1.71

2.54

29.46

77.30

1.96

1.13

74.79

3.54

83.63

4.34

97.04

66.25

1.53

2.S6

1.32

1.31

.26

.42 5.18

1.13

.72 70.57

70.50

2.53

HOIS

7.88

7.11

7.20

1.36

1.27 7.56

7.83 7.68

8.30

7.98

7.62

7.46

2.68

7.41

2.99

3.64

6.85

6.55 6.13

6.11

6.76

6.98

6.32

5.81

6.06

5.76

2.92

7.61

3.15

8.07

7.79

3.71

5.72

5.80

5.35

5.49

5.43

5.12

4.93 1.39

1.40

2.85

3.30

4.50 5.70

S.20

3.60

2.60

5.10

7.65

8.03

9.01

7.76

5.00

7.09

7.17

7.29

7.73

7.43

7.46

5.33

1.49

7.79

9.35

8.13

3.39

5.59

6.17 6.03

6.09 6.40

1.31

1.43

5.72

6.40

6.48

6.26

6.2S

2.97

3.71

6.18

6.76

7.14

6.65

3.34

3.57

6.07

6.83

6.96

6.47

6.83

3.23

3.87

5.83

6.52

6.63

6.69

6.05

2.82

S.91

5.as 3.96

3.98

6.26

6.S3 5.56

5.48

2.75

3.65

5.55

5.63

5.09

2.70

5. SO

S.S3

2.13

5.33

2.74

5.43

2.43

3.04

5.IS

5.72 6.09

5.66

5.63

5.96

5.99

5.79

4.52

3.10

3.38

5.89

VM CV SULPHUR

. ---. ---------" -----• ----" ----. ----------. ------. ----. -. ----_ ---13.73

41.83

41.40

10.89

11.02

40.53

8.21

19.39

11.89

41.47

41.13

40.76

40.23

9.SI

19.41 41.07

41.15

41.09

41.22 9.86

16.10

41.57

41.09

40.92 40.86

40.56 B-25

22.63

41.98

41.03

42.06

40.35

40.48

6.89

41.56

40.67

12.46

24.34

40.34

40.40

42.35

41.93

6.29

7.77

41.86

41.94

30.61 17.07

40.78

40.30

18.02

39.96

12.23 39.67

8.32

21.44

41.81

41.25

40.95

41.59

41.72

41.27 39.34

40.47

11.53

13.83

14.69 10.36

--------------" ----------" ---" . ----. -. ----. -. --. -----. . ---. -. ---1055

7224

7375 7339

7337

7483

-2337

7341

7376

7373

7080

7301

783

2119

7174

7284

7246

7181

614

135S

7269 7218

7276

687 3

7280

365

2328

73S9

732S

7336

7082

7375

25

7381

7274

1004

3312

7172

7302 7527

74S2

25

3 360

7337

5039

417 7236

7360

571 7147

29 7056

27

2670

7269

7233

7253

72S9 7371

7321

6658

7326

7652

1S41

139S

7092

.43

.38

.25

.43

.84

.37

.19

.13

.15

.33

.31

.29

.19

.30

.43

.05

.30

.34

.33

.36

.21

.32

.19

.24

.27

.33

.42

.40

.18

.16

.28

.24

.20

.16

.17

.15

.29

.30

.28

.19

.46 2.02

.11

.21

.16

.17

.16

.17

6.50

2.25

1.18

.33

.46

2.95 1.73

.85

.25

.20

.17

.24

.34

.10

.44

.19

.13

4.06

2.00

.54

.37

.41

.41 1.84

1.46

1.59

.34

.39

.20

.29

.40

4.14 1.87

.51

.36

.39

.32

3.82

1.80

.45

.37

.30

.35

.25

4.23

1.45

.30

.24

.21

.23

.20

.52

.49 3.59

3.65

.63

.39

.33

.33

.33

.12

.37

.39

.91 3.22

.47

.25

.46

.23

.64

.27

.15

2.72 .71 .33 .21 .16 .21 .22 .15 .13 .12 .14

1.34

.73

DDH EASTING

O3500 96882.57

C3500 96882.57

C3S00 96883.57

C3S00 96883.57

C3500 96862.57

C3502 86341.08

C3503 96341.08

C3503 96341.08

C3502 96341.08

C3503 96341.08

C3502 96241.09

C3502 96341.09

C3507 98733.33

C3507 98733.33

C3S07 98733.33

C3507 98733.33

C3507 98733.33

C3507 98733.33

C3507 99733.33

C3531 98343.19

C3531 98345.19

03531 68348.18

C3531 99349.19

C3531 98349.19

C3531 58348.19

C3531 98349.19

C3S31 98349.15

C3531 38349.19

03531 98345.16

C3531 99349.19

C3531 99349.19

C3536 97599.90

C3536 97599.90

C3536 97533.90 C3S36 97555.30

C3536 97595.80

C3536 37599.50

C3536 57599.90

C3536 97599.90

C3536 97593.90

C3538 38236.55

03538 38336.95

C3539 96336.95

C3539 98226.95

C3S39 98226.95

C3538 88226.95

C3538 88226.55

C3538 56226.95

C3536 98236.95

C3S39 97655.50

C353S 57655.50

03535 97655.50 C3539 97655.50

C3539 97655.50

C3539 57655.50

C3539 87655.50 C3535 97655.50

C3575 35085.38

C3575 86085.38

C3575 86089.38

C3575 99099.39

03575 99089.38

C3576 99109.86

C3576 99109.86

C3576 99109.86

C3576 96109.96 C3S76 99109.96

C3576 99109.96

C3S34 97914.93

C3634 97914.53

C3634 97914.53

C3634 57514.53

C3634 57514.53

C3634 57514.53

C3634 57914.93

C3634 97914.93

C3634 97914.53 C3634 57514.53

C3634 57514.93

C3635 57751.18

C3635 87751.18

C3635 97751.18 C3635 97751.16

C3635 87751.18

C363S 97751.18

C3637 88228.17

C3637 58238.17

C3637 56338.17

C3637 88338.17

C3637 98338.17

C3637 36338.17

C3637 38228.17

C3637 38228.17

C3641 37652.57

C3641 37652.57

C3641 37652.57

C3641 37652.57

C3641 37652.57

C3641 37652.57

03641 37652.57

C3653 86216.27

C3639 96216.27

03663 96216.27

C3699 96216.27

C3699 56216.27 C3636 56216.27

03702 56365.54

C3702 66385.84

C3702 56385.34

C3702 36385.34

C3702 96395.94

C3703 96385.64

C3704 86356.81 C3704 96356.81

03704 96356.81

03704 96358.81

C3704 96358.81

C3704 96358.81

C3704 56358.81

C3706 66811.46

C3706 56811.46

O3706 96811.46

C3706 96911.46

C3706 96911.46

C3706 96811.46

C3882 58561.81

03882 99561.91

C3882 98561.91

C3982 99561.81

C3887 99611.68

C3887 86611.68

C3867 88611.68

NORTHING SAMP. Ho.

194751.26 SNCH140O5

134751.26 SNCM14006 154751.26 SNOM14007

194751.26 SNCM140O8 164751.26 SNDB14010

184604.16 SNDT14011

154604.16 SNCM14012

194904.16 SNCM14013

194904.16 SNCM14014

194904.16 SNCM1401S

154504.16 SNCH14016

194904.36 SNCM14017

195314.32 SNDT14032

195314.32 SNOM14033 195314.32 SNCM14034

195314.32 SNCH14035

195314.32 SNOM14036

195314.32 SNCM14037

195314.32 SNCM14038

195633.20 SNDT14046

195633.30 SNCM14047

155633.20 SNCM14048

155633.20 SNCM1404S

195633.20 S N C M H 0 5 0

155633.20 SNCM140S1

195633.30 SNCH14052

195633.20 SNOM14053

195633.20 SNCH14054

195633.30 SNCH140S5

165633.30 SNCM14056

155633.30 SNDB14057

154610.31 SNDT14066

194610.21 SNCM14067

194610.21 SNOM14069

194610.21 SNCM14065

194610.21 SNOH14070

194610.21 SNDBI4071

194610.21 SN 14072

194610.21 SN 14073

194610.21 SN 14074

194619.80 SNDT14083

134616.80 SNCM14084

154615.80 SNCM1408S

184619.80 SNCM14086

194639.90 SNCH14087

194615.80 SNCH14088

154615.80 SNCH14085

194616.80 SNCM14090

194619.80 SNDB14091

194332.46 SNDT14097

194332.46 SNCM14099

194332.46 SNCH140S9 154332.46 SNCM14100

194332.46 5NCM14101

194332.46 SNCK14102

194332.46 SNCH14103 164332.46 SKDB14104

158841.57 SNDT14206

158841.57 SNCM14207

158641.57 SNCM1420S

158641.57 SHDB14205 198641.57 SN 14214

198449.05 SHDT14213

198448.05 SNCM14213 158448.05 SNCH14215

186448.05 SNOH14216

188448.05 SNCM14217

188448.05 SNDB14218

194629.83 SNDT34341

154628.83 SNCH14342

154628.83 SNCH14343

194628.33 SNCK14344

194628.83 SNCH14345

154628.83 SNCH14346

154628.83 SNOM14347

194628.83 SNCH14348

184628.83 SNCH14349 194628.83 SNCM143S0

194628.83 SNOM14351

154501.68 SNDT14388 154901.66 SNCM14389

194901.69 SNCM14390

194901.65 SNCH14351

194901.69 SNCM14392 194501.65 SNOH14393

194612.61 SNCH14362

194612.61 SNCM14363

194612.61 SNCM14364

194612.61 SNCH14365

154612.61 SNCH14366

164612.61 SNCM14367

154612.61 SNCH1436B

154612.61 SNDB14369

154325.76 SNDT14429

154325.76 SNQD.4431

154325.76 SNOM14432

154325.76 SNCM14433

194325.76 SNCM3.4434

194325.76 SNOH14435

194335.76 SNDB14436

195257.48 SNDT14S33

155257.48 SNCM14S34

155257.48 SNCH14535

195257.48 SNCM14536

195257.48 SNDB14S37 195257.48 SNDB14S39

195335.72 SN 14S5S

195335.72 SN 14556 195335.72 SN 14557

195335.72 SN 14558

18S33S.72 SN 14SS9

165335.72 SN 14560

15S625.85 SNDT14589

195625.55 SNCM24S90

195625.95 SNC1C4S91 195625.95 SNCH14S92

195625.55 SNCM14594

155625.65 SNDB1455S

1SS625.S5 SNDB14SS6

195490.90 SNDT14561

195490.80 SNCM14563

195430.30 SNCX14S64

135450.90 SNCH14566

195490.80 SNDS14S69

195450.80 SHDB14S70

155263.45 SNDTI4766

155263.45 SNCH14768

155263.45 SNCM1476S

155263.45 SNDB14771

155332.57 SNDT14790

135332.97 SNCM147 91

195332.97 SNDB14793

DEPTOP

27.940

29.630

28.720

30.720 32.180

20.720

20.820

21.500

33.600

23.400

24.400

25.400

16.310

16.710

17.640

48.380

15.380

50.380

51.350

22.600

22.700

21.200

25.700

27.200

28.400

28.660

25.780 30.030

30.160

31.520

32.720

72.030

73.130

73.630

75.130

76.S30

79.340

75.640 75.740

75.840

63.820

B3.920

95.230

B6.330

87.500

88.100

88.410

50.890

91.600

58.530

58.620

59.620 60.620

61.620

53.620

63.560 64.060

34.120

34.220

36.230

38.290

39.530

37.690

38.030

11.030

13.530 14.170

44.670

177.550

177.650

178.150

178.870

178.870

180.870

181.870

183.870

183.870

181.870

185.650

140.450

140.550

111.050

113.050

143.330 114.560

81.140

84.350

BS.600

86.660

87.850

68.030

50.060

91.350

58.100

56.700

55.700

60.700

63.500

63.050

S3.550

47.310

47.410

50.080 53.150

53.660 54.180

38.830

38.530

11.810

13.810

15.600

16.100

76.480 76.580

78.000

78.580

B3.3S0

84.300

S4.800

56.560

57.670

55.670

63.870

67.030

66.120

48.570

49.370

50.990

54.240

48.620 48.720

52.180

DEPBOT

28.930

29.720

30.720

31.680

32.280

20.820

21.500

22.600

23.400

24.400

25.400

26.620

46.710

47.640

48.380

48.380

S0.280

51.350

52.300

22.700

24.200

25.700

27.200

23.400

25.660

25.780

30.030

30.160

31.520 32.720

32.820

72.130

73.630

75.130 76.520

76.340

75.640

79.710

75.840

78.840

83.820

85.330

86.230

67.500

88.100

35.410

60.850 91.600

91.700

58.620

58.630

60.620 61.620

62.620 63.560

64.060 64.160

34.230

36.230

38.290

38.970

41.030

38.030

39.530 42.530

44.170

44.670

44.770

177.650

178.150

178.870

175.870

180.870

181.870

182.370

183.870

184.870

185.550

166.600

140.550 141.050

142.0S0

143.220

144.560

144.850

B4.250

85.600

86.660

B7.8S0 B8.030

90.060

91.250

91.850

58.200

59.700

60.700

62.500

63.050

63.550

63.650

47.110

50.090

52.150

53.680

51.180

51.280

38.330

41.810

43.810

45.600

46.100

46.200

76.580

78.000

73.530

60.170

84.300 64.800

84.500

56.660

55.670

61.670

66.130

60.130

S8.220

48.670

50.530

53.420

54.340

48.720

51.360

52.280

RD ASH

1.38 10.50

1.31 1.64

1.32 2.56

1.31 1.12

2.54 63.35

2.08 60.87

1.33 1.62 1.30 .50

1.30 .48

1.32 .50

1.32 .42

1.33 2.21

1.41 15.36

1.31 .36

1.25 .92

1.29 .51

1.29 .38

1.25 .53

1.28 .63

2.41 80.63

1.31 4.15

1.31 1.33

1.30 1.08

1.31 1.30

1.36 6.58

1.68 57.04

1.32 3.05

1.85 53.80

1.31 2.12 1.34 5.46

2.31 78.76

1.85 48.90

1.31 3.55

1.30 1.01

1.33 4.45

1.31 1.80

1.30 1.S9

2.07 63.35 2.30 78.50

1.38 12.86

2.54 85.75

1.31 2.89

1.30 3.21

1.30 2.33

1.31 6.88

1.29 .81

1.25 3.58

1.58 38.48

2.68 88.58

2.51 77.07 1.32 5.70

1.28 .47

1.28 .42

1.30 2.56 1.30 .67

1.31 1.75 2.32 74.43

2.33 77.24

1.36 5.62

1.31 4.23

2.46 80.40

1.25 .21

1.55 56.99

1.31 2.00

1.29 .30

1.30 1.48

1.39 12.91

2.47 84.86

1.97 55.22

1.32 4.56

1.30 1.75

1.25 1.33

1.31 .32

1.28 1.07

1.39 1.54

1.30 .46

1.38 1.11

1.28 1.30

1.46 24.50

2.15 75.50

1.35 1.47

1.31 3.27 1.25 .59

1.31 1.44

1.44 11.IS

1.28 .88

1.26 .59

1.28 2.34

1.26 .40

1.27 1.16

1.30 .96

1.32 8.33

1.59 37.45

2.17 56.87

1.28 0.30

1.26 0.42

1.29 0.53

1.31 1.60

1.30 1.64

2.60 82.24

2.10 64.38

1.30 1.02

1.33 4.38

1.32 1.52

1.30 1.72

2.51 85.05

2.04 60.32

1.32 3.27

1.26 0.27

1.32 1.88

1.30 0.85

3.06 65.56

1.65 36.37

1.33 3.32

1.31 3.46

2.58 85.63

1.33 2.10 1.31 2.63

0.46 83.13

2.51 83.26

1.30 1.53

1.30 1.41

1.31 1.27

1.30 1.86

2.55 86.51

2.56 86.73

1.30 3.15

1.34 8.67

2.54 68.12

2.18 74.06

1.33 6.17

2.26 77.87

MOIS VM

5.77 36.53

5.73 11.38

6.15 39.66

5.97 41.47

3.33 9.48

1.03 18.88

6.01 10.88

6.13 43.19

6.71 41.31

5.33 40.37

7.07 40.87

6.73 40.45

4.45 35.60

5.00 35.29

5.06 40.08

5.17 40.03

5.01 40.82

1.85 40.27

4.14 41.68

3.72 8.84

5.25 35.43

5.49 40.58

5.41 40.19

5.26 40.14

5.81 37.22 3.54 20.17

5.40 39.63 3.96 20.32

6.00 38.46

5.58 37.93

3.01 10.38

3.84 23.09 4.57 42.01

5.66 40.69 5.05 41.34

5.36 41.27

5.37 40.43

4.26 16.79

3.13 11.14

4.09 37.94

3.37 8.41

4.49 39.29

4.61 40.93 4.25 42.13

1.59 39.70

1.68 41.SS

3.53 43.34 3.60 28.60

2.85 7.14

2.34 13.05

3.35 42.13

4.55 41.63

1.88 40.95

4.60 41.23

4.88 40.96

5.23 39.06 4.67 11.82

4.01 1.34

5.21 38.09

4.33 40.68

3.05 11.02 6.03 41.51

4.74 20.IS

5.77 10.15 5.56 41.85

5.58 41.05

4.49 37.04

2.37 4.11

2.79 21.81

3.65 42.30

4.22 42.19 4.73 41.41

5.32 41.00

1.75 42.17

1.48 41.59

5.15 41.49

5.00 40.61

4.78 41.15

3.14 34.77

.67 10.85 4.30 41.51

4.15 41.60 1.15 12.41

4.14 42.42

1.07 41.39

4.53 40.03

4.74 46.03

4.15 42.44

S.16 40.93 4.85 41.39

4.S3 63.81

3.14 42.05

3.37 27.53

2.43 18.59

1.07 43.14

5.03 41.29

1.61 11.63

1.42 40.76

3.67 40.01

3.86 8.25

3.75 18.64

6.69 41. SS

7.50 36.54 7.25 41.44

6.76 41.53

2.92 8.86

3.01 20.37

6.22 41.00

S.83 41.12 6.56 41.09

6.40 41.41

3.16 16.59

3.82 30.39

5.69 42.34

6.12 41.46

3.04 8.71

6.88 40.49

6.20 40.60

2.90 9.21

2.44 9.96

5.26 41.80

5.19 42.24

5.04 40.51

4.52 42.52

1.91 8.58

3.34 3.34

4.57 40.76

4.15 38.55

2.18 7.03

2.71 14.58

4.32 35.57

2.02 12.30

CV SULPHUR

65S1

7303

7130

7348

403

2166

71S6

7366

7352

7180

7251

7095

6369

7319 7550

7S55

7591

7506

7532

611 7138

7332

7351

7315

6936

2743

7217

3281

7305

706S

960

3429

7406

7454

7133

7386

7421

2033

852 S573

6 7402

7 447 7407

7062

7S66

4954

7536

13

926 7259

7586 7570

7 463 7538

74 1027

-6679 7256

-7402 _ 7249

7434

7320

6561

--7277 7222

7379

7260

748S

74S6

7487

7445

7205

5805

7447

7317

7SS0

7503 6166

7508

7629

7492

7613

7532

7549

7243

457 4

7614

7544

7567

7468

7420

-7228

6877

7136

718S

. 2326

7061

7323

7172

726S

-443S

7135

7209

-7080 7143

-7343

7310

7323

7419

--7330 6892

--7113 .

.54

.19

.18

.30

.94

1.16

3.73 1.73 .72 .16 .39 .36

.32

.32

.29

.33

.21

.21

.19

.28

.26

.15

.15

.16

.16

.17

.15

.20

.17

.17

.19

3.36 1.51 .53 .23 .20 .24 .08 .16 .26

.15

.54

.23

.16

.24

.23

.15

.21

.08

6.70 2.35 .56 .84

1.10 .7 9 .63 .50

.26

.26

.28

.78

.15

.66

.20

.23

.17

.44

.38

5.22 1.10 1.S4 1.18 .50 .55 .46 .43

1.00 .20 .32

1.06 .61 .19 .17 .28 .14

.45

.27

.20

.17

.17

.14

.33

.25

7.32 1.70 0.82 1.08 0.59 0.52 0.24

3.09 0.90 0.23

0.19

0.23

0.34

4.11

1.19

0.26

0.26

0.29

0.24

0.05

0.40

0.18

0.18

0.15

0.20

0.15

3.05

0.2S

0.14

0.14

0.17

0.37

0.30

0.35

0.15

0.16

0.15 0.37

0.05

Appendix 6.7 (confd)

DON EASTING

P3093 55600.30 P3033 99600.90 P2093 55600.30 F3093 99600.90 P3093 99600.30 P2093 99600.90

P2444 96510.02 P2444 96510.02 P2414 96510.03 P3444 96510.03 P2444 96510.02 P2444 96510.02 P2444 96510.03

P244S 98S19.33 P3445 98518.33 P3445 96519.33 P344S 98518.22 P244S 99518.32 P3445 98518.33

P3711 99136.99 P3711 99136.58 P2711 99136.98 P2711 99136.38 82711 99136.98 P2711 99136.38 P3711 99136.98 P3711 93136.98 P37U 99136.98 P3711 99136.98 P27U 99136.98 P2711 99136.98

P2712 98519.49 P2712 38519.49 P2712 96519.43 P2713 98519.49 P2712 98519.49 P2712 98519.49 P2713 98519.49 P2712 38519.49 P2712 33513.49 P2712 98519.43

P3713 98850.83 P3713 98850.83 P2713 98850.33 P2713 38850.83 P2713 58850.83 P2713 98850.83 P2713 98850.83 P2713 98850.83

P2717 96479.44 F2717 96479.44 P2717 96479.44 P2717 36473.44 P2717 36473.44 P2717 96479.44 P2717 96479.41 P3717 96173.44 P3717 96479.44 P3717 96479.44

P3734 97434.99 P2724 97434.99 P2724 97434.99 P2724 97434.39 P2724 97434.99 P2724 97434.99 P2724 97434.99 82724 97434.93 P2724 57434.35 P3734 97434.55 P3734 97434.95 P2721 97434.99 P2724 97434.99 P2724 97434.99 P2724 97434.33

P2726 38566.68 P2726 88558.66 P2726 58538.68 P2726 98999.68 P3736 98338.68 P3736 98998.68 P2726 98938.68

P2760 99081.77 P2760 35083.77 F2760 99081.77 P2760 99081.77 P2760 96081.77 P2760 55081.77 P2760 55081.77 P2760 99081.77 P2760 95081.77 P2760 99081.77 P2760 99081.77 P2760 99081.77 P2760 99081.77 P2760 99081.77 P2760 99081.77 P3760 35081.77 P3760 35061.77 P3760 35081.77

P3317 99760.34 F3217 987C0.34 P3217 98760.34 P3217 98760.34 P3217 98760.31 P3217 98760.31 P3217 98760.34 P3217 387 60.3 4 P3217 38760.34 P3217 98760.34

P3213 38805.44 P3218 38808.44 P3213 38803.44 P3213 58503.44 P3213 98305.44 P3216 96909.44 F3219 98909.44 P321S 58805.44

P3221 98896.33 F322I 38896.33 F3221 36896.33 F3331 98986.33 F3221 98896.33 F3221 96896.33 F3221 98896.33 F3221 99896.33 F3221 98896.33

P3222 98822.34 P3222 38822.34 P3222 98822.34 F3222 96822.34 F3222 98822.34

F3224 98755.56 F3224 98755.56 F3224 98755.56 F3224 98755.56 F3224 98755.56 F3224 38755.56

NORTHING

203801.00 303901.00 203901.00 203801.00 302801.00 302801.00

195505.69 19S50S.69 195505.69 195505.65 195505.69 195505.69 155505.69

195333.06 195333.06 155333.06 155333.06 195232.06 155333.06

195506.89 195506.99 195506.86 155506.89 155506.83 135506.89 195506.99 195506.89 195506.89 195506.98 195506.89 155506.89

195498.53 135498.53 155456.53 155458.53 195498.53 195438.53 135459.53 155458.53 195498.53 195498.53

155856.31 135856.31 135856.31 135856.91 195856.91 195856.91 135856.31 135856.31

135006.06 155006.06 195006.06 195006.06 135006.06 135006.06 195006.06 195006.06 195006.06 195006.06

154740.31 164740.31 154740.31 134740.31 194710.31 194740.31 194740.31 194740.31 194740.31 194740.31 194740.31 194740.31 194740.31 134740.31 134740.31

138805.84 138805.84 138805.84 138805.84 186805.84 188805.84 138805.84

195305.61 195305.61 195305.61 195305.61 195305.61 195305.61 195305.61 195305.61 155305.61 155305.61 155305.61 155305.61 155305.61 155305.61 135305.61 195305.61 195305.61 195305.61

195447.99 19S447.98 195447.99 19S447.99 195447.98 195447.38 195447.38 135447.58 155447.58 155447.58

155155.73 155155.73 155155.73 195455.73 155455.73 155455.73 135455.73 135455.73

155575.03 135575.09 155575.03 155575.09 195575.09 19557 5.09 195575.05 155575.05 155575.09

195138.03 195136.03 195139.03 195138.02 195128.02

195066.52 195066.52 195066.52 155066.52 195066.52 195066.52

SAMP. NO.

SN 10064 SN 10065 SN 10066 SN 10067 SN 10069 SN 10069

SNOT10S62 SNCM10563 SNCM10S64 SNCM10565 SNCM2 05 66 SNDB10567 SNDB10566

SN 10572 SN 10573 SN 10574 SN 10575 SN 10576 SN 10577

SNDT11170 SNDT1117I SNDT31372 SNDT11173 SNCM11174 SMDB1117S SNDB11176 SNDB11177 SNDB11178 SNDB11179 SNDB11180 SNDB11181

SNDT11182 SNCM11183 SNCM11284 SNCMX118S SNCMD1185 SNCM11186 SNCH11187 SNCM111B8 SNDB11189 SNDBDU89

SNDT13390 SNCM111S1 SNCM111S2 SNCH11163 SNCM11194 SNCM11195 SNCM111S6 SNDB11157

SNDT11206 SNCM11207 SNCHI1206 SNCM11205 SNCM11210 SMCM11211 SNCH11212 SNDB11213 SND811214 SNDBD1314

SNDT11254 SNDT11255 SNDT11256 SNDT11257 SMDTH358 SNDT11259 SNCM11260 SNCM11261 SNCM11262 SNCM11263 SNCM11264 SND811265 SNDB11366 SNDB11367 SNDB11368

SNDT113S0 SNCM11281 SNCM11282 SNCM11283 SNCM11284 SNCM1128S SNDB11286

SN 31346 SN 11347 SN 11348 SN 11346 SN 11350 SN 11351 SN 11352 SN 11353 SN 11354 SN 11355 SN 11356 SN 11357 SN 11358 SN 11358 SN 11360 SN 11361 SN 11362 SN 11363

SNDT12961 SNDT12962 SNDT12963 SNDT12964 SNCM12365 SNCM12566 SNOH12567 SNCM12S69 SNDB12S65 SNDB12970

SNDT13978 SNCM1397 9 SNCM13980 SNCM12381 5NCM139S2 SNDB13683 SNDB12984 SNDB12385

SNDT12557 SNCM125S8 SNCM12SS5 SNCM13000 SNOM13001 SNCM13002 SNCM13003 SNCM13004 SNDB13005

SNDT13007 SNCH13008 SNCM1300S SNCM13010 SNCM13011

SN 13014 SN 13015 SN 13016 SN 13017 SN 13018 SN 13019

DEPTOP

51.100 51.300 53.570 53.840 55.360 56.600

65.090 85.260 86.710 88.970 90.610 92.300 93.410

16.160 16.260 17.030 19.400 52.030 53.600

19.140 18.310 18.920 19.140 19.320 20.770 20.910 21.240 21.400 21.770 21.900 22.120

37.400 37.560 37.630 38.360 33.360 38.760 38.600 10.380 10.570 10.S70

22.070 22.170 22.350 22.770 23.890 21.960 25.900 27.250

66.870 87.020 67.370 88.590 85.720 81.140 52.040 92.750 94.300 94.300

50.790 50.890 51.690 52.060 52.440 52.600 S2.770 54.000 55.250 56.450 57.640 58.030 58.330 53.300 60.250

57.330 57.490 58.400 58.480 60.810 61.600 62.500

6.610 6.710 7.040 7.130 7.580 7.640 7.500 6.400 6.500 5.400 8.600 10.400 10.500 11.400 11.900 12.950 13.450 14.000

38.540 38.640 39.080 39.260 39.650 11.130 12.060 13.150 14.520 45.430

17.660 17.930 18.610 51.490 52.480 53.370 53.710 54.970

31.540 32.040 32.400 33.720 34.320 35.300 36.370 37.830 38.120

26.140 26.500 28.230 30.500 31.340

7.510 7.610 8.310 8.650 3.500

10.350

DEPBOT

51.300 52.570 53.840 55.360 56.600 57.430

85.260 86.710 88.870 30.610 32.300 93.410 93.510

16.360 17.030 13.400 53.030 53.600 53.700

18.310 18.930 13.140 19.330 30.770 30.310 31.240 21.400 21.770 21.300 33.120 22.220

37.580 37.630 38.360 38.760 38.460 39.600 40.380 10.570 10.780 10.670

22.170 22.350 22.770 23.880 24.360 25.800 27.250 27.400

87.020 87.370 88.550 85.720 91.140 92.040 92.750 94.300 94.460 94.400

50.990 51.690 52.060 52.440 52.600 52.770 54.000 55.250 56.450 57.640 59.030 58.930 59.500 60.250 60.350

57.490 58.400 58.480 60.310 61.600 62.500 62.600

6.710 7.040 7.130 7.360 7.640 7.500 8.400 8.500 9.400 9.900 10.400 10.900 11.400 11.500 12.950 13.450 14.000 14.300

38.640 39.080 39.260 39.650 41.130 12.060 43.450 44.920 45.430 45.530

47.930 18.610 51.190 52.180 53.370 53.710 54.870 55.070

32.040 32.400 33.720 34.920 35.900 36.970 37.950 38.120 38.220

28.500 29.230 30.500 31.340 32.310

7.610 8.310 8.650 3.500 10.350 10.340

RD

1.71 1.33 1.33 1.32 1.32 1.30

1.60 1.32 1.32 1.31 1.33 1.32 2.22

2.23 1.40 1.32 1.30 1.25 2.64

3.42 1.33 2.30 1.45 1.33 2.30 1.50 2.67 1.40 1.33 1.40 2.61

2.47 1.58 1.36 2.60 2.60 1.35 1.31 1.31 2.00 2.00

2.S3 1.43 1.36 1.35 1.30 1.29 1.39 3.13

2.26 1.33 1.30 1.30 1.30 1.30 1.33 1.30 2.44 2.44

2.44 1.34 1.3S 1.36 1.49 2.34 1.30 1.23 1.30 1.3S 1.33 1.37 1.34 1.30 3.33

2.60 1.32 1.31 1.31 1.29 1.32 2.S5

2.46 1.37 2.07 1.35 2.15 1.49 1.35 1.33 1.35 1.36 1.40 1.36 1.38 1.36 1.39 1.32 1.30 1.66

2.49 1.36 2.49 1.48 1.31 1.30 1.31 1.31 1.60 2.61

I.SI 1.36 1.30 1.31 1.30 2.23 1.37 2.48

2.31 1.38 1.31 1.33 1.31 1.31 1.30 1.53 3.35

1.39 1.31 1.32 1.32 1.32

2.53 1.32 1.43 1.30 1.S0 1.3S

ASH

40

37

2 1 3 3

72

73 13 2

1 88

80 6 75 18 1

73 25 38 13 56 14 86

83 31 10 67 67 g l I S2 62

65 16 8

2 67

69 4

1

1 3 1 33 33

67 6 7 10 20 76 1 1

5 3 8 7 3

77

B7 1

1 4

72

81 9 64 4

66 22 2

2 36

83 7 63 21 1

1 1

35 B9

26 6

1 73 11 82

77 B 1

1 26 72

11 1

1 2.

66 2 21 1

23 7

90 90 .50 .SO .50 80

40 60 60 20 40 00 30

00 00 90 30 20 80

90 20 50 70 10 00 00 00 20 00 10 30

60 30 60 00 00 30 30 60 80 80

80 20 20 50 40 40 10 50

30 60 70 20 40 30 00 10 10 10

20 60 40 70 40 20 20 20 40 30 30 40 30 30 20

80 50 40 50 00 30 60

70 90 30 60 40 30 10 10 10 20 10 10 10 30 10 70 20 80

IS SO 25 90 90 68 85 32 87 80

57 67 90 81 06 74 20 74

80 30 10 70 80 B8 40 60 90

70 80 80 30 50

98 28 57 10 16 41

NOIS VM C

5.60 -7.10 -7.50 -7.90 -7.50 -7.40 -

1.70 -5.60 -5.70 -5.60 -5.40 -5.20 -3.30 -

J.30 -4.20 -1.20 -1.10 -3.50 -1.50 -

3.20 -1.10 -3.60 -1.00 -4.60 -2.50 -4.00 -2.20 -1.50 -3.60 -4.70 -2.20 -

3.40 -1.30 -1.10 -3.00 -3.00 -1.30 -1.10 -1.10 -2.80 -2.80 -

3.20 -3.80 -1.60 -S.30 -S.30 -5.00 -1.60 -3.10 -

3.10 -5.10 -5.70 -S.50 -fi.SO -S.40 -5.50 -6.50 -S.10 -3.10 -

2.40 -1.20 -1.50 -4.60 -4.70 -1.00 -5.60 -S.30 -5.60 -S.30 -5.80 -5.80 -1.20 -1.10 -3.10 -

2.80 -5.30 -6.00 -5.60 -5.10 -4.80 -3.10 -

3.50 -5.20 -4.00 -5.SO -4.30 -4.80 -7.10 -S.70 -7.10 -7.80 -S.50 -7.SO -6.10 -6.10 -S.20 -6.10 -4.70 -4.30 -

3.10 -4.02 -3.03 -3.76 -4.63 -5.03 -4.81 -1.30 -3.02 -1.56 -

1.04 -4.50 -4.47 -1.S6 -4.43 -2.64 -3.67 -3.34 -

3.10 -4.10 -4.20 -4.50 -3.92 -4.64 -3.30 -3.50 -3.20 -

3.50 -4.10 -4.35 -4.30 -3.50 -

1.72 -4.35 -3.32 -1.53 -3.51 -3.83 -

CV SULPHUR

2.37 1.84 .61 .28 .28 .31

6.12 1.22 .34 .14 .15 .22 .15

.13 .22 .23 .19 .16 .19

.16

.41

.35

.07

.07

.23

.16

.19

.18

.15

.54

.16

.25

1.32 .47 .35 .29 .26 .29 .30

.89

.50

.32

.31

.30

.19

.IS

.22

.28

.50

.65

.56

.36

.34

.26

.30

.68

.45

.25

.50

.20

.20

.17

.16

.20

.33 2.33 .73 .30 .30 .23 .37 .25

1.S0 .46 .23

1.36 .68

1.58 .40 .38 .25

DDH EASTING NORTHINO SAMP. No. DEPTOP DEPBOT RD

P3234 88755.56 195066.53 SN F3324 98755.56 195066.52 SN F3224 99755.56 195066.52 SN

13020 13021 13022

P3388 P3388 P338S P3388 P3389 F3388 P3388 P3398 P3388 P3388 F3388

97515.52 97515.52 97515.52 97515.52 97515.52 97515.52 97515.52 97515.52 97515.52 97515.52 97515.52

195087 195087. 195087 195087 135087. 135087. 135087. 195087. 195087. 135087. 195087.

69 SNDT13441 69 SNCH13442 88 SNCH13443 88 SNCM13444 88 SNCH1344S 63 SHCM13446 83 SHCM13447 89 SNCM13448 89 SNDB13449 88 SNDB13450 85 SNDB13451

10.940 11.600 12.600

116.320 116.560 117.340 119.500 113.500 130.500 131.130 131.310 133.330 133.500 122.750

11.600 12.600 12.700

116.560 117.340 118.500 119.500 130.500 131.120 131.310 122.330 122.500 122.750 122.850

1.34 6.48 1.32 5.63 1.58 33.76

2.56 85.68 1.34 4.72 1.31 .74 1.31 .80 1.30 .87 1.32 .66 1.60 32.79 1.30 2.26 2.63 88.56 1.31 4.46 2.40 81.32

MOIS VM

3.89 -3.90 -3.25 -

3.09 -4.38 -4.79 -4.84 -4.97 -4.94 -4.03 -1.37 -

CV

.

. -_ -------

SULPHUR

.39

.29

.16

.07

.39

.16

.11

.15

.15

.15

.16 1.91 1.30 2.83 .03

F31S8 56632.97 195082.38 SNDT13855 55.190 59.290 2.46 77.51 3.34 12.44 795 4.01 P3498 96622.97 P3498 96622.97 F3498 86622.57 P3458 86622.97 F3498 96622.37 P3498 96622.97

195082.38 SNCM13896 195082.38 SNCM13997 195082.38 SNCH13558 185082.38 SNCM13SS3 195082.38 SNCH14000 195082.38 SNCM14001

P3520 99008.64 395098.01 SNCM14042 P3520 99008.64 195098.01 SNCM14043 F3520 99008.64 195099.01 SNDB14045

C3997 C3897 C3857 C3897 C3897 C3887 C3887 C3887

SNDT14807 SNCH14806 SNCM14809 SNCM14S10 SNCH14811 SNCM14812 SNCM14813 SHDB14811

59.390 60.790 63.390 63.670 65.270 66.770

34.420 25.830 30.060

22.100 22.200 23.440 23.740 26.500 27.680 28.200 28.460

60.750 62.290 63.670 65.270 66.770 68.020

25.830 27.280 30.160

22.200 23.440 23.740 26.500 27.680 28.200 29.450 29.550

1.31 1.30 1.31 1.32 1.30 1.32

.57 1.40 1.53 1.87 .64

3.51

5.74 41.53 6.10 41.01 6.16 41.54 6.06 41.12 S.53 40.63 5.83 38.95

7329 7277 7250 7162 7316 7137

1.30 1.61 1.29 .53 1.86 62.46

2.67 82.31 1.31 2.41 1.31 3.31 1.31 0.54 1.31 0.82 1.36 12.71 1.64 38.78 2.35 84.65

1.71 40.17 7423 4.12 42.74 7632 3.32 17.13 2257

2.16 12.13 -4.13 39.81 7479 3.75 42.03 4.90 41.31 1.71 10.43 3.75 38.5B 2.63 27.68 1.94 8.62

.29

.30

.39

67 25

7460 1.2S 7535 0.46 7514 0.3S 6658 0.38 4488 0.47

0.21

• Depth of top of Sangatta seam. . Depth of bottom of Sangatta seam. • Relative density (g/cm3). . Ash yield (adb. 4}. . Moisture content (adb, t). • Volatile natter content (adb, 4).

CV • Calorific values (adb.cal/g). SULPHUR . Sulphur content (adb, 4).

DEPTOP DEPBOT

ASH MOIS

Appendix 6.8 Ash composition and ultimate analytical data for the Sangatta seam.

DDH

C2061

C2063 C2089 C2194 C2246 C2264 C2271 C2282 C2290 C2320 C2329 C2331 C2332 C2334 C2343 C2442 C2517

C2518 C2519 C2521 C2522 C2552 C2553 C2554 C2555 C2556 C2579 C2585 C2635 C2646 C2670 C2693 C2694 C2695 C2696 C2810 C2811 C2812 C2915 C2916 C2917 C2918 C2919 C2920 C2921 C2922 C2923 C2995 C2996 C3145 C3394 C3395 C3396 C3397 C3399 C3400 C3401 C3409 C3410 C3411 C3443 C3444 C3445 C3449 C3451 C3454 C3500 C3502 C3536 C3575 C3631 C3634 C3635 C3637 C3699 C3706 F2093 F2444 F2711 F2713 F2717

F2724 F2760

EASTING

99090.20

99429.40 98776.40 104845.60 98788.70 99086.46 99910.38 97370.20 96712.31 98873.24 98904.90 96330.61 96716.63 98519.88 98388.37 97689.39 98835.53

98221.68 97739.81 97612.29 97661.33 96514.24 96296.45 96074.91 96831.13 97102.74 96110.64 98058.92 98722.02 98728.14 98544.59 99111.17 99105.11 98986.89 98950.65 99060.52 99029.85 99036.07 98777.81 98726.09 98469.41 98506.21 98532.18 98360.91 98431.88 98194.13 98380.44 98990.72 99047.45 98509.85 99295.60 99265.07 99131.79 99168.54 98644.70 99505.51 97613.91 99004.14 97617.33 97617.91 99916.22 100025.77 99260.97 98520.40 98380.51 98763.63 96882.57 96241.08 97599.90 99089.38 98019.06 97914.93 97751.18 98228.17 96216.27 96811.46 99600.90 96510.02 99136.98 98850.83 96479.44 97434.99 99081.77

NORTHING

201766

201141 197896 205527 195847 198701 204130 195055 194932 195054 200228 195022 195565 195243 197435 196985 195505

194515 194243 194761 195438 195987 194759 195750 195233 194754 195500 195009 198249 198581 195956 195404 195294 195355 195841 195293 195272 195328 195251 195366 195373 195625 195766 195741 195880 195519 195128 195434 195453 195120 202023 201483 201020 200526 200254 203237 195127 195767 195127 195129 203758 204219 203019 200570 200008 199768 194751 194904 194610 198841 194863 194628 194901 194612 195257 195490 202801 195505 195506 195856. 195006. 194740 195305.

50

50 91 59 50 20 00 59 09 50 41 41 30 70 88 42 30

27 47 20 36 34 31 89 52 34 66 44 95 69 77 17 34 97 73 38 63 05 .09 94 .88 16 11 .59 .97 .44 30 .44 83 03 05 06 63 55 97 34 88 42 55 94 02 38 03 17 55 66 27 16 20 56 55 83 69 61 48 80 00 69 39 91 06 31 61

SiO,

0.0 49.6 43.5 29.2 37.6 Q.O

29.3 44.3 45.9 65.2 60.5 30.0 52.5 59.3 28.0 32.0 41.0

39.5 41.0 49.8 38.7 0.0

36.0 58.5 37.7 40.0 40.7 57.4 52.5 65.5 42.5 58.0 50.5 31.5 41.4 41.0 45.0 31.5 47.6 46.3 58.9 45.0 60.2 51.1 37.2 21.2 32.0 54.5 57.5 56.0 53.0 22.3 53.0 40.0 29.0 39.3 57.5 34.0 61.0 0.0

56.5 45.0 28.5 41.5 55.0 53.0 55.5 55.6 50.5 36.5 23.0 27.5 16.5 31.0 56.3 33.6 25.2 31.0 42.2 56.8 40.0 56.0 37.0

ALjO, Fe,0, TiO, CaO MgO

0.0 0.0 20.8 20.3 24.6 22.5 17.8 28.9 27.0 23.2 0.0 0.0

9.21 18.5 18.3 15.8 24.2 17.3 21.1 9.08 21.2 13.9 18.5 15.0 17.2 5.30 28.4 7.8 15.9 14.4 13.8 13.2 22.8 15.6 31.0 15.9 23.6 25.0 21.4 9.74 17.5 8.2 0.0 0.0

28.5 28.2 21.9 10.9 20.9 6.32 23.8 10.4 28.8 17.2 22.0 5.50 25.3 14.0 19.0 9.9 28.3 20.0 19.0 17.6 20.5 24.0 19.8 39.0 27.7 21.6 26.5 25.5 32.0 8.45 23.5 40.3 36.3 S.25 30.0 13.9 23.9 9.87 29.5 12.5 22.1 6.5 16.7 18.2 30.1 10.9 18.9 13.7 26.5 27.0 25.5 6.05 24.0 9.40 29.5 4.95 32.5 9.1 17.0 43.0 16.3 26.4 16.5 33.0 21.5 36.3 27.0 19.2 14.5 20.0 12.3 45.0 20.0 12.0 0.0 0.0

16.3 19.8 13.1 28.6 11.0 19.4 22.4 27.0 34.0 1.75 27.8 11.2 28.1 9.11 29.2 7.87 28.8 13.4 28.5 55.6 13.5 13.3 19.3 10.4 9.65 9.5 20.5 12.8 27.0 9.5 14.5 19.0 13.1 33.8 17.7 9.35 21.5 28.6 29.0 10.3 8.0 47.0

18.8 5.90 39.5 11.5

0.0 0.70 0.69 0.51 1.22 0.0 0.46 0.88 0.97 0.91 0.86 0.62 0.61 1.20 0.36 0.53 0.64 0.76 0.88 0.98 0.56 0.0 0,84 1.12 0.77 0.77 0.84 0.92 0.65 0.96 0.75 0.77 0.75 0.75 0.34 1.11 1.46 0.66 0.82 0.79 0.95 0.86 0.75 0.48 0.71 0.57 0.71 0.70 0.94 0.96 1.08 0.85 0.69 0.58 0.81 1.03 0.69 0.41 0.91 0.0 0.77 0.60 0.33 0.80 1.15 1.06 1.05 1.02 1.25 0.17 0.63 0.73 0.30 0.77 1.08 1.33 0.37 0.51 0.63 0.87 0.47 0.61 0.94

0.0 2.28 1.29 7.53 1.85 0.0 13.4 4.63 1.81 0.28 0.37 10.8 10.0 0.34 14.5 14.8 5.8

1.65 0.75 6.40 17.5 0.0 1.34 1.80 11.5 5.85 3.35 3.62 0.89 0.52 0.69 0.49 0.71 1.0

2.10 0.84 2.76 0.36 0.70 0.80 0.91 2.23 2.68 1.74 4.43 17.5 3.85 3.95 0.75 1.49 0.99 3.50 1.0 1.81 2.40 3.50 0.99 1.53 0.78 0.0 1.28 4.20 7.8

1.48 0.81 1.41 0.93 0.97 0.39 0.73 16.4 10.0 34.4 14.3 0.70 5.78 5.59 12.4 0.99 0.83 0.59 4.68 3.50

0.0 2.07 3.04 5.92 2.05 0.0 8.79 6.38 3.18 0.82 0.93 7.66 7.0

0.41 10.9 10.1 6.16 4.40 1.80 5.10 4.96 0.0 0.80 1.28 9.28 3.15 4.30 2.98 1.96 1.55 4.30 1.93 0.98 0.78 1.03 0.48 3.10 0.55 0.95 3.08 2.35 4.32 2.75 3.62 5.65 11.0 4.08 3.73 3.13 2.04 1.45 7.6 0.69 4.90 5.1

2.60 2.60 1.70 2.53 0.0 1.43 5.5 9.7

3.45 0.51 0.75 1.40 1.56 1.27 0.94 14.6 11.9 14.5 8.2

1.15 8.91 5.05 10.9 2.45 1.25 1.48 4.30 0.88

»a,0 K20 P2Oj Mn,0« SO

0.0 0.88 1.11 0.79 1.95 0.0 0.55 2.10 2.10 0.46 0.43 3.20 1.38 0.50 1.50 2.20 1.91 3.25 3.27 1.80 1.84 0.0 3.10 1.50 2.33 2.24 3.21 3.22 1.10 1.43 1.94 0,96 1.19 4.75 3.93 1.02 1.08 0.85 1.09 1.26 0.65 1.35 0.80 3.81 3.09 1.09 2.07 0.75 0.94 1.48 0.41 0.83 1.13 0.93 2.73 0.91 0.90 2.78 0.53 0.0 0.36 0.44 8.5 1.30 0.54 2.45 0.64 0.73 0.67 1.43 4.15 4.85 2.63 2.06 1.20 2.89 5.47 3.10 0.54 1.33 2.33 1.24 2.77

0.0 0.92 0.98 1.17 1.14 0.0 0.96 1.33 1.23 2.12 1.93 1.49 0.85 1.64 0.40 0.89 1.25 1.76 1.93 0.93 0.87 0.0 1.21 0.63 1.22 1.36 1.98 3.95 1.50 2.60 1.09 2.55 2.38 0.72 0.58 1.57 1.95 1.15 1.85 1.50 2.90 1.48 1.98 0.90 1.17 0.53 0.75 1.91 2.91 1.80 2.40 0.78 1.11 0.90 0.48 1.85 2.38 0.52 2.44 0.0 1.93 1.19 1.0 1.10 1.93 0.62 2.29 2.47 2.46 0.4O 0.49 1.25 0.21 0.55 2.63 0.87 0.63 1.10 1.16 1.23 0.59 2.18 1.10

0.0 0.28 0.17 0.85 1.90 0.0 0.59 0.45 0.82 0.33 0.32 0.31 0.18 0.20 0.14 0.33 0.13 0.19 0.19 0.09 0.11 0.0 0.38 0.38 0.10 0.65 0.17 0.02 0.09 0.01 0.33 0.10 0.15 0.18 0.14 0.35 0.69 0.33 1.0

0.19 0.51 0.38 0.16 0.26 1.35 2.4

0.29 0.39 0.57 0.13 0.36 0.57 0.17 0.44 0.47 4.31 0.14 0.34 0.13 0.0 0.21 0.14 0.11 0.29 2.30 0.32 0.26 0.25 0.27 0.07

0.43 0.88 0.56 1.66 0.70 0.29 0.60 0.59 0.05 0.05 0.11 0.54 0.75

0.0 0.05 0.03 0.16 0.07 0.0 0.21 0.15 0.09 0.01 0.01 0.01 0.01 0.01 0.05 0.04 0.01 0.03 0.08 0.13 0.02 0.0 0.04 0.02 0.01 0.04 0.05 0.02 0.02 0.04 0.06 0.03 0.07 0.12 0.02 0.05 0.04 0.07 0.04 0.04 0.06 0.02 0.01 0.04 0.O3 0.03 0.10 0.05 0.03 0.01 0.01 0.11 0.01 0.07 0.07 0.08 0.11 0.04 0.06 0.0 0.12 0.21 0.06 0.08 0.05 0.01 0.0 0.0 0.0 0.07 0.03 0.03 0.03 0.02 0.01 0.09 0.90 0.O4 0.16 0.02 0.05 0.03 0.04

c

0.0 0.55 0.31 5.74 0.12 0.0 16.8 5.08 0.57 0.05 0.10 11.0 6.27 0.03 12.1 10.6 5.23 0.06 0.06 5.5 8.30 O.O 0.20 0.20 8.61 10.6 0.75 2.20 0.15 0.05 0.25 0.05 0.25 0.20 0.10 0.10 1.90 0.10 0.18 0.40 0.40 1.34 2.25 1.21 3.46 11.5 2.81 4.05 0.33 1.95 0.40 3.11 0.25 0.90 1.87 1.05 0.75 1.23 0.55 0.0 0.55 2.16 12.9 1.10 0.25 0.33 0.72 0.32 0.86 0.40 15.3 13.4 10.8 9.1

0.10 12.3 7.38 14.6 0.65 0.10 0.50 4.68 0.45

H

77.9 71.6 74.3 76.4 80.4 80.3 77.6 79.9 80.2 80.1 78.5 73.5 78.8 79.8 79.3 80.2 80.7 80.0 80.0 80.0 79.7 79.9 79.8 79.9 79.6 79.9 79.2 79.5 79.3 79.8 80.6 79.9 80.4 80.6 80.4 80.3 30.2 80.1 80.5 79.7 80.2 80.3 79.2 B0.4 80.5 80.6 80.1 80.4 80.2 B0.1 78.9 79.1 79.1 79.2 79.6 78.9 79.9 80.6 80.1 80.1 77.9 78.1 79.6 79.0 79.4 80.5 80.64 30.32 82.31 30.4 80.3 80.4 79.7 76.6 79.0 77.11 78.1 79.1 B0.7 80.5 80.3 79.6 77.7

N

5.40 4.93 5.26 5.55 5.74 5.81 5.52 5.71 5.70 5.62 5.62 5.43 5.69 5.60 5.28 5.88 5.46 5.71 5.44 5.91 5.46 5.41 5.61 5.70 5.74 5.71 5.82 5.76 5.75 5.92 5.69 5.34 5.47 5.78 5.87 5.83 5.89 5.76 5.63 5.61 5.63 5.55 5.71 5.71 5.58 5.68 5.49 5.71 5.62 5.79 5.45 5.22 5.54 5.26 5.62 5.44 5.34 5.58 5.40 5.40 5.20 5.49 5.51 5.51 5.62 5.73 4.52 4.65 4.84 5.55 5.64 4.72 5.86 5.52 5.55 4.91 5.37 5.64 5.45 5.87 5.65 5.93 5.12

S

1.86 1.50 1.47 1.61 1.62 1.31 1.37 1.42 1.36 1.75 1.84 1.49 1.48 1.59 1.93 1.45 1.47 1.59 1.46 1.46 1.62 1.29 1.32 1.46 1.34 1.54 1.51 1.78 1.54 1.57 1.63 1.86 1.75 1.54 1.79 1.65 1.59 1.53 1.65 1.66 1.60 1.59 1.79 1.87 1.63 1.56 1.89 1.49 1.64 1.52 1.36 1.47 1.7

1.50 1.59 1.48 1.81 1.92 2.01 2.05 1.30 1.92 1.60 1.76 1.85 1.60 1.24 1.34 1.37 1.82 1.59 1.50 1.61 1.85 1.55 1.38

1.48 1.41 1.97 1.70 1.46 1.49 1.60

0.37 0.20 0.27 0.25 0.22 0.26 0.64 0.17 0.53 0.65 0.50 0.84 0.30 0.24 0.21 0.18 0.20 0.55 1.20 1.54 0.19 0.94 0.94 0.32 0.28 0.41 0.31 0.25 0.26 0.22 0.25 0.25 0.67 0.34 0.25 0.59 0.26 0.81 0.28 0.18 0.25 0.19 0.20 0.21 0.24 0.18 0.25 0.23 0.24 0.14 0.27 0.20 0.41 0.24 0.27 0.55 0.18 0.27 0.23 0.24 1.64 0.28 0.61 0.23 0.26 0.20 1.02 0.36 1.43 1.83 0.24 0.80 0.18 0.24 1.74 0.22

0.62 0.43 0.39 0.25 0.74 0.35 0.55

o co, py SUL ORGS

14.24 0.23 0.0 0.06 0.0 0.06 16.19 0.31 12.02 0.10 12.32 0.08 14.87 0.33 12.80 0.45 12.21 0.11 11.88 0.08 13.5 0.05

13.74 0.32 13.73 0.99 12.77 0.17 13.28 0.44 12.2 0.49

12.17 0.30 12.1 0.19

11.90 0.10 12.09 0.75 13.03 0.87 13.21 0.39 12.33 0.03 12.62 0.11 13.04 0.77 12.44 0.32 13.1 0.17 12.71 0.24 12.65 0.07 12.56 0.31 11.83 0.19 12.15 0.44 11.61 0.20 11.74 0.02 11.69 0.06 11.63 0.02 12.06 0.17 11.80 0.06 11.9 0.07

12.85 0.16 12.32 0.47 12.37 0.27 13.10 0.47 11.81 0.15 12.0 0.21

11.98 0.59 12.27 0.18 12.17 0.44 12.30 0.25 12.45 0.11 14.02 0.03 14.01 0.19 13.25 0.04 13.80 0.09 12.92 0.12 13.63 0.15 12.77 0.35 11.63 0.03 12.26 0.31 12.21 0.21 13.96 0.08 14.21 0.08 12.68 0.05 13.5 0.13 12.87 0.05 11.97 0.09 12.58 0.22 13.33 0.24 10.05 0.30 10.40 0.16 12.23 0.59 11.58 0.38 12.65 0.97 15.79 0.61

12.16 0.01 14.70 0.0

14.43 0.10 13.42 0.68 11.49 0.58 11.68 0.12 11.85 0.07 12.63 0.41 15.03 0.02

0.04 0.07 0.05 0.05 0.08 0.O7

0.11 0.06 0.07 0.26 0.26 0.13 0.04 0.06 0.02 0.01 0.01 0.14 0.21 0.03 0.01 0.01 0.14 0.12 0.03 0.04 0.12 0.01 0.04 0.04 0.05 0.02 0.17 0.13 0.04 0.36 0.01 0.53 0.01

0.02 0.0 0.0

0.01 0.0 0.0 0.0

0.04 0.0 0.0

0.02 0.15 0.05 0.18 0.08 0.07 0.07 0.02 0.07 0.12 0.01 0.21 0.05 0.04 0.05 0.01 0.01 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

0.09 0.0

0.10 0.02 0.11 0.04 0.09 0.07 0.01

0.01 0.01 0. 01 0.01 0.01 0.01 0.02 0.01 0.02 0.03 0.03 0.02 0.01 0.01 0.01 0.01 0.01 0.02 0.03 0.01 0.01 0.01 0.02 0.01 0.01 0.01 0.01 0.01 0.03 0.01 0.01 0.01 0.03 0.01 0.02 0.02 0.01 0.03 0.0

0.01 0.0 0.0

0.01 0.0 0.0 0.0

0.01 0.0 0.0

0.01 0.01 0.01 0.18 0.01 0.01 0.01 0.01 0.01 0.01 0.01 0.02 0.01 0.01 0.01 0.01 0.01 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

0.01 0.0

0.01 0.01 0.01 0.01 0.03 0.02 0.04

0.29 0.13 0.22 0.16 0.13 0.16 0.45 0.10 0.40 0.29 0.16 0.62 0.23 0.16 0.18 0.16 0.18 0.35 0.88 0.47 0.16 0.16 0.71 0.16 0.23 0.33 0.15 0.21 0.17 0.16 0.17 0.21 0.42 0.18 0.18 0.17 0.23 0.19 0.0

0.15 0.0 0.0

0.17 0.0 0.0 O.O

0.19 0.0 0.0

0.11 0.15 0.13 0.19 0.14 0.18 0.42 0.14 0.18 0.08 0.22 1.26 0.20 0.52 0.16 0.21 0.18 0.0 0.0 0.0 0.0 0.0 0.0 0.0 0.0

1.47 0.0

0.46 0.37 0.24 0.18 0.56 0.22 0.45

Notes:

RV = Pyritic sulphur. SUL = Sulphate. ORGS = Organic sulphur.

Appendix 7.1 Drill hole data for the Al seam, Bukit Asam Coalfield

DDH

WB4J17

WB-Q18

WB-019

WB4123

WBJS1S

WB4T26

WB4J27

WB4J28

WB4J30

WD-OOI

TVB-002

WB4X15

WB-0O6

WBfl07

WBJTO

WB4W9

WBfllO

WB-011

WB-012

WB-013

WB-015

WB-016

WB4J2P

WB-03!

WB4T32

TA4T25

TA-032

TA-IBJ

TA-036

TA-039

TA4M1

TA-046

TA-047

TA4157

GP-602

GP-003

AL-I

AL-3

AL-4

ALo l\L*

AL8

AL-9

AL-12

AL-14

AL-I3

AL-17

AL-24

AL-ll

AL-13

BD-2

BD-3

HD-4

WB4343

AR-1

AR-3

AR-4

AR-6

nc-to RC-11

RC12

RC-12A

RC-14

FC-I7

RC-21

RC-22

RC-23

RC-26

RC-27

RC-27A

RC-2S 1

RC25>

RC-29A

RC-XA

RC-32

RC34 }

BC-35

RC-37

RC-38

RC-39

RC-40 1

KC-41 1

BASTWO

a

365051

363731

363769

363770

36«Z3

364865

363888

3*4557

364046

363994

3635SS

364729

364534

364599

364646

364846'

364045

364396

364546

364900

363971

364232

ZHOU

364301

364180

364646

364119

364042

364953

363889

364101

363900

364237

364380

36471.5

364262

364395

364094

363971

-J64J62"

3*4190

364003

364196

363920

364013

363963

364669

364371

363760

364201

364993

364*31

364756

363040

364326 1

364290

364176

364597

364463

364133

363730

363729

364725

364008

363397

364014

363909

363790

363960

363939

364129

364454

364432

364860

363507

'364095

364809

363617

363203

364844

365083 |

3M32Z9 i

NORTHMO

m

9587328

9587124

9586914

9586521

9586641

9586433

9586027

9385740

9585592

9383803

9333334

9585261

9386281

9585936

9587842

95X7718

9587597

L 9587454

9387635

9387312

9587376

9587244

9383045

9585006

9585224

9586144

9336134

93*6531

9386336

9386712

9586898

9587394

9387734

958609!

P5S7I57

9587444

9387319

9587333

9586684

958634J

9586744

9387010

9587014

9586371

9386956

93S8S37

9527760

9587287

9586692

9586238

9387343

9387768

9584911

9586620

9355674

9584324

9385563

9585473

953520S

m&3\ 9585406

9383445

9585399

9383693

9385798

9585864

9335923 _ j

9386036

9586078

9386055

P53602D

9586001

9386008

9X1999

9386088

986219

9586132

9586434

9586360

9336311

9336335

9386311

ELEV

ra 5020

7590

76.90

65.80

6003

76.70

68.70

6720

76.80

BSSO

82.40

80.80

39.40

75 JO

33.70

4].ou

50.40

56.70

44.10

49 00

64.60

4820

97.60

88.40

93 JO

73.70

6340

81.10

8320

74.90

6780

5830

4360

70.80

73.80

6680

6320

3760

7130

6'3-JiI

70.40

71.10

67.00

68 SO

67.00

963)0

45 49

6120

78.70

67.40

45.40

40.80

30.80

6020

64.10

91.40

69.10

6890

S6SI

8287

101.63

99.44

78.54

89.07

7834

7785

78.84

79.64

67.37

6821

6S.JB

6682

6651

1999

7322

4283

8524

36.14

61.12

84.13

73.23

0262 1

THICK

m ta 8.58

827

886'

823

9.12

6.44

7.53

7.13

750

3.76

3.10

7.54

765

8.78

9.03

952

5.86

7.86

968

85a

4.51

Alt

626

7.80

7.41

3.60

693

8 31

7.67

366

9.15

956

8.14

133

6.75

5.50

820

523

3"JU

3S0

660

• 8.00

830

200

350

6.30

6.X

600

7J0

10.40

11.23

1250

10.40

ASH

% 760

800

7.10

6.70

8.40

7.50

880

720

750

268

730

2.00

7J0O

650

750

8.80

8.70

16.80

720

7.10

11.90

1320

730

7.70

2J11

3.00

490

450

3D0

SULPH

% 0.60

051

055

053

055

0.44

050

0.73

039

0510

0.44

0.46

0.70

0.75

0.87

053

038

060

054

064

057

0.77

050

121

0.47

061

051

065

057

3DO

J.19

1S1

2.70

3O0

920

T.6U

12-50

930

1380

3.80

230

3.40

3.20

3.80

250

2.60

3.60

2 60

7.T0

660

930 I

3.80

730

690

6.43

6.10

4.10

085

2.80

7.13

423

750

5.65

8.40

41 X

0.49

0.92

0.84

DDH

BD-5

BD-6

BD-7

W-l

TA-023

TA-024

TA-029

TA-030

TA4731

TA4333

TA-056

TA435S

TA-059

TA4J63

TA-064

TA-065

AP-22

AP-21

AP-23

AA-1

AA-2

AAJ

S-?«

S-l

5-2 c t 0-J

AP-15

AF-I7

GP-004

GP-O03

OF-006

GP-007

OP-OOS

OF-010

CP-011

GP-013

AA-4

AA-5

AL-2

AL-r

AL-IO

NM-1

SM-1

WB4333

WB-034

WB-030

j WB4B7

1 WB4J3S

i WB4T39

| WB-040

050

0.60

1.64

720 1

7.45

7.45

7.10

805

7.25

tSi

290

110

8.40

0.85

8.85

880

8.20

943 1

W M 41

VVB4342

RC-42

RC-44

RC-45

RC-46

RC-46A

RC-47

RC-47A

RC-48

RC-JO

RC-50A

HC-3I

RC-51A

RC-53

RC-54

RC-55

RC-55A

FC-36A

i | RC-57

6.43

722

12*j

609

724 j

1

050

0.42

05"5

052

055

RC-58

RC-59

RC-39A

RO60

RjJ-6'1

RC-62

RC-62A

RC-63

RC-63

RC-70A

EAST7NO

m

364902

364768

364669

364617

363305

363636

364329

363938

363783

303936

364143

364456

363912

364687

364394

364255

364239

364255

363820

364339

364310

364429

364297

364304

364369

364293

364032

363983

364080

364310

363982

363734

363732

364135

3643S5

364936

364456

364485

| 364375

StstWSl

3*3814

364325

363814

364556

364427

363037

364343

363932

364679

365219

363642

363333

364759

363263

364143

364210

364207

363010

363047

364178

365027

365096

364138

364136

364163

364931

365144

363082

363774

364116 ]

364135

365116

365140 ""

364179

364301

365151

365113

364601

364201

364300 1

NORTHINO

m

9586712

9586602

9537746

9586241

9586706

9386684

9583648

9383988

9536179

9380333

9535508

9585333

9585729

9383919

9534943

9584878

9535361

9585337

9585545

9584992

9385039

9384973

P3350P7

9385268

9534867

9585815

9533492

95344J2

9386133

' 9386045

9583938

9383312

9585815

9585677

9385901

9586129

9534933

9381892

9387307

vwcrrj-i

9587034

9585183

9585340

9587718

9588242

9356S63

9587666

9586981

9386357

9587019

9536972

9386360

ELEV

ra 56.00

6120

4630

7530

7420

8130

7180

79.60

72330

6420

81.20

7650

10020

80.80

102.10

95.40

6800

8390

9010

9820

10080

102 DO

ST 00

93.10

10730

10350

7230

9830

62.70

6970

8060

9650

100 SO

79.80

66.70

79 70

101.10

9130

3350

035.711

78.40

7720

10300

3650

5550

3640

5350

6930

7160

5550

82.40

62.60

THICK

ra 820

1053

7.75

957

830

856

768

750

628

730

774

4.80

726

8118

2.70

250

7D0

650

680

5.75

4.75

5.16

649

600

450

454

550

05U

855

733

830

535

3.84

7.70

750

5.15

5.42

5.41

5.00

05D

1.70

3 00

050

634

9D0

9.44

920

6.72

573

9.12

9.14

800

! 9386450

9586869

9536723

9536736

9386741

9536605

9386394

9586806

95S6747

9336830

933KS9S

9586903

9536995

9586923

9586923

9586998

9587277

17337118

9587089

9587157

9587204

9537374

«874(4

9587404

9537414 a

9533OO0

9588203

9588380

61.06

84.68

61.05

4188

41.81

1133

3463

4950

55.70

51.00

6567

6662

61.75

3356

48.70

5027

63.00

6iSS

5963

49.70

4352

6023

34.14

44 OS

46 20

39 19

5566

3259

6.90

930

565

5.15

4.00

930

9.40

520

7.75

9.45

453

3.70

545

7.00

930

0.75 ~l

820

5.45

5S5

7.00

$31

623

575

10.25

S.70

930

925

ASH

% 250

230

2.30

1.95

690

6.69

620

660

5.00

330

6.60

750

7.60

7.70

320

100

SULPH

%

0.45

0.47

0.71

050

053

073

056

039

!5>5

0.40

130 j

f'

|

2.00

569

386

526

226

208

146

221

2.18

053

0.76

108

033

059

064

0.43

0.33

I 3.00 ]

2.43 '

5.05 (

1

940

7.70

10O0

880

3.70

1130

2.40

6.X

115VI

864

12.10

11.26

032

051

02.1

0.44

031

0.88

0.79

032

0J6

021

058

0.43

1

4.83 0.13

[

i

12.72

1151)

1056

5.94

769

0.67

08)-

0.18

063

029

9.20 i

i 1

Appendix 8.1 " Z O N E D KRIGING" procedure in coal reserve assessment.

Depositional model.

Depoositional environment of coal seam is modelled on the basis of the study of interseam

clastic sedimentology, coal seam geometry and thickness/quality spatial variation. This step

is to locate different zones that have different seam geometry and thickness/quality

characteristics (geological zoning).

Collecting data from each zone.

This includes collecting, preparing and posting geological and thickness/quality data in each

zone to be able to analyse statistically.

Basic statistical analysis for coal data from each zone.

This step involves basic statistical display (histogram, probability graph, mean, variance,

coefficient of variation etc.) and outliers check. The types of population for each coal

parameter are determined in this step; and it will guide the use of subsequent geostatistical

analysis.

Variogram analysis.

This step is to determine the spatial structure of coal parameters in each zone. It will

involves the spatial variability, continuity (range), trend and isotropy of the parameters. The

structural elements of the variograms (e.g. nugget effect, sill, and range) are used in

subsequent kriging process.

Kriging.

This includes point kriging interpolation for contouring the values of coal data and block

kriging for calculating the reserve (with defined estimation variance).