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Lin lidhzv! . f 2 . hm :3: ,p E. its? z. I :34! Tl £531? 3 aCX>l » M: enzfippqogyrfgg; ; ‘7' 1-411!“ % LIBRARY l E‘fifict‘aigan a”. 1 University l r. w This is to certify that the dissertation entitled interpreting crystal Kinetics of drowth Ancient Dolomites presented by Lisa Ann Kessels has been accepted towards fulfillment of the requirements for PhOD. Geological sciences degree in Major professor Date 8 [%(&Z MSU is an Affirmative Anion/Equal Opporrunigr Institution 0-12771 PLACE IN RETURN BOX to remove this checkout from your record. To AVOID FINES return on or before date due. MAY BE RECALLED with earlier due date if requested. DATE DUE DATE DUE DATE DUE 6/01 c:/C|F|CJDateDua.p65-p.15 INTERPRETING CRYSTAL GROWTH KINETICS OF ANCIENT DOLOMITES BY Lisa Ann Kessels A DISSERTATION Submitted to Michigan State University in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY Department of Geological Sciences 2001 - In.“ § 1 . .r .. o i . '1 a. -. w. . a. .f. . 1 Q y 3. .4 I I .utfi x d .. J 5 an . II.» I u . J c A 5 _ t. i 1 . ‘54 - M“. . . H. . i u.. i w. . _ ...v 4 . I. .s _ . a 1 «I. b .n V a. A ‘1 t. ‘ i Fl v .\. . 1 ,fi . , H a. p“ i . Au 1 .l. u t i \- v . g to r» , ... I, g . 0;. h: -, ., H ,.. s a . m. .. a T u . , I n I I I IL. L H .. T. “J , .i. _ C i Na r ;I Q , r. . . .r. L n, D). t, ‘ I, 4. . J. r. r. _\ . . .( .T t J i . H. .. .. 3 . 4. .. 1. “(Hi ;\v A m ' an ‘ ~ 1 di- tut .\ J as g ajnams11fl ‘J CHTYMWI ‘d INTERPRETING CRYSTAL GROWTH KINETICS OF ANCIENT DOLOMITES By Lisa Ann Kessels AN ABSTRACT OF A DISSERTATION Submitted to Michigan State University in partial fulfillment of the requirements for the degree of DOCTOR OF PHILOSOPHY Department of Geological Sciences 2001 Professor Duncan F. Sibley iluimimmmmmm ABSTRACT INTERPRETING CRYSTAL GROWTH KINETICS OF ANCIENT DOLOMITES BY Lisa Ann Kessels Crystal growth has been described by the following models; 1) mononuclear growth model, 2) birth and spread growth model, 3) polynuclear growth model, and 4) spiral growth model (Christian 1972, Nielson 1964, Ohara and Reid 1959, Burton et al. 1951). In order to apply these growth models to ancient dolomite reservoirs, an estimate of the growth rate is necessary. The zone width in concentrically— zoned, luminescent dolomites can be used to estimate growth rate (Nordeng and Sibley 1996, Carlson 1989, Kretz 1974, 1973). By rearranging the equations for the known growth models, crystal population trends on a zone-width vs. crystal-size plot can be constructed to distinguish between groups of crystals growing by mononuclear growth versus the following mechanisms: 1) polynuclear growth, 2) birth and spread growth, 3) diffusion-limited and 4) spiral growth mechanisms. To determine the extent that any group of crystals within a dolomite unit grew by the same crystal growth mechanism, samples were examined at regular intervals from three luminescent dolomites: l) Saluda and Whitewater Formations (Ordovician), Indiana, U.S., 2) Burlington—Keokuk Formation (Mississippian) Missouri, U.S., and 3) Seroe Domi , ~ _ Ebrmation ”diocene), Curacao, Netherland Antilles. Plots of zone‘widtli‘vs. crystal-size for crystals in an individual sample‘wemxa constructed. Crystal growth equations fitted to each sample's zone-width vs. crystal-size plot were compared among samples from: 1) the same lithology and formation, 2) different lithologies and the same formation, 3) the same lithology and different formations and 4) different lithologies and different formations. Analysis of crystal growth equations from all three dolomites indicate a linear relationship, dr/dt = k'r, where growth rate increases with crystal size (r) indicating crystal growth mechanism does not vary on the outcrop scale with lithology, BBC, SmO, or age of formation. The average slope (k’) of all three dolomites was 0.181. Correlation coefficients for the equation dr/dt = kr ranged from 23% to 81%. Zone-width vs. crystal-size plots constructed for pairs of crystals adjacent to each other in the Saluda and Burlington-Keokuk formations revealed the same growth mechanism dr/dt = k'r, indicating growth was controlled by a crystal surface process instead of solution variability. u .-‘-.' “3"70hloto.v ACKNOWLEDGMENTS I VKNlld like to thank and acknowledge Duncan Sibley or his guidance and.patience over the years. I would also ike to thank the members of my committee, Mike Velbel, lave Long and Tom Vogel. Their insights and comments have >roved invaluable. I am also deeply indebted to Bruce ‘ouke for thin section samples and locations for the Seroe )omi Formation samples. Last, but not least, I would like .0 thank Eldon who saw me through to the end. iv iilliiflflg TABLE OF CONTENTS List of Tables List of Figures Introduction Reaction Rate Crystal Growth Mechanisms in Natural Systems Combination of Crystal Growth and Solute Flux Population Trends for Crystal Growth Mechanisms Geologic Setting Burlington-Keokuk Formation Seroe Domi Formation Saluda/Whitewater Formations Methods Zone Selection Sampling locations Zone Measurements Geometric Corrections Statistical Methods Results Comparison of Crystal Growth Rate Equation among Lithologies of the Same Dolomite Comparison of Crystal Growth Rate Equation between Different Dolomites Temporal Comparisons within the Seroe Domi Vii xii 10 20 25 27 35 35 42 50 71 71 73 80 86 9O 91 112 113 Formation Comparison of Crystal Growth Equations for Adjacent Crystals in Thin Section Discussion Crystal Growth Equation and Crystal Growth Mechanism Spatial and Temporal Crystal Growth Trends Variance in Crystal Growth Equations Conclusions Appendix A Appendix B Bibliography 114 114 116 119 127 130 132 135 145 237 able able able able able able able able able able able able able able able able able able 10. 11. 12. 13. 14. 15. 16. 17. 18. Radial Growth Rate Equations for Crystal Growth Summary of relationship between crystal size and increment of new precipitate Carbon and Oxygen Isotope Data for Saluda and LIST OF TABLES Whitewater Formations Samples with normal crystal size distributions at the 95% confidence interval Samples with normal zone width distributions at the 95% confidence interval Samples with normal distributions at the 99% confidence interval Slope and correlation coefficients for all samples Parameters to distinguish Case I, Sample List for Saluda Formation Hwy 421 Outcrop Sample Sample Sample Sample Sample Sample Sample Sample Sample M1 Measurements M2 Measurements M4 Measurements M8 Measurements M11 Measurements M20 Measurements M21 Measurements M26 Measurements M28 Measurements vfi II and III 8 14 58 97 98 99 101 139 146 147 148 149 150 151 152 153 154 155 I a. r , . . . . a .. . 1 i 1 c s .. . u... . . A n .. n .. e. x . . c . .— . a . _ .5 7— ..~ :4 .4u «1.. «(a «44 f1 4 an .a" a... .a.. .=.. ..... e. .o.. ..... a... J. a. Pu .. u‘ ... w. w.“ .. .N .u. Du kw .. s . . o . u . . . y . . . e . v . - . - t u... u... Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table 19. 20. 21. 22. 23. 24. 25. 26. 27. 28. 29. 30. 31. 32. 33. 41. 42. Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample M30 Measurements M34 Measurements M42 Measurements G1 Measurements GB Measurements G4 Measurements G5 Measurements G6 Measurements G7 Measurements G8 Measurements D6 Measurements D8 Measurements D10 Measurements D12 Measurements SD3 Measurements SD7 Measurements SD11 Measurements SD13 Measurements SD15 Measurements SD23 Measurements P2 Measurements P5 Measurements P17 Measurements P19 Measurements 156 157 158 159 160 161 163 164 165 166 167 169 170 171 172 173 175 176 177 178 179 180 181 182 , 3a '- m” J1; 1,55 ‘L l‘ i i q r -fl EEG: ‘37 ’5' A k 4h 9.; 5.. 1,, ., I g ’ Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table 43. 44. 45. 46. 47. 48. 49. 50. 51. 52. 53. 54. 55. 56. 57. 58. 59. 60. 61. Sample Sample Sample Sample Sample Sample Sample Sample Sample P27 P31 P34 P36 P37 P40 P41 Measurements Measurements Measurements Measurements Measurements Measurements Measurements P45 Measurements List for Saluda Formation Highway 7 and Highway 56 Outcrops Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sal R-l Measurements Sal Sal Sal Sal Sal Sal Sal Sal Sal Sal Sal R-5 Measurements R-10 A-ld A-5d A-7d A-Sg A-7g 56-1 56-5 Measurements Measurements Measurements Measurements Measurements Measurements Measurements Measurements Measurements Measurements Pay—1 Measurements Pay-5 Measurements ix 183 184 185 186 188 189 190 191 192 193 194 195 196 197 198 199 200 202 203 204 205 206 207 Y" {awdnix ” L ? r~ ‘ fit“ } K I - ‘d r f. Amn'n‘ . 7 .353 | ’. ' 3 . L 1 Hi. I L ' f\ ’1’ ‘1“ z; r L s "\ '1 3114.74” :71. '7 ‘ -‘UuYJ7Utwr’1i: a. it .‘ °'£m -(.r: ' . w 31 4.11 ‘ u r‘ ‘ "1 J ~ _, I I J 7." ML .1 ‘I 'n J " .1“ r’. 1' i . r r . _, .-N a ' I'. ‘44. \V! 1" fl . . . .~ Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table Table 66. 67. 68. 69. 70. 71. 72. 73. 74. 75. 76. 77. 78. 79. 80. 81. 82. 83. 84. 85. 86. 87. Sample Sample Sample Sample Sample Sample Hwy 61 Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Sample Pay-ll Measurements Ton-11 Measurements Sal How-1 Measurements Sal How-6 Measurements Sal 7—8 Measurements List for Burlington-Keokuk Formation Outcrops DFS-l Measurements CAR-5 Measurements MIN-6 Measurements LAK-lO Mesaurements MIN-16 Measurements DFS-15 Measurements DFS-24 Measurements LAK—22 Measurements MIN-29 Measurements LAK-31 Measurements DPS-32 Measurements LAK-36 Measurements DFS-37 Measurements LAK-4O Measurements DUNC—56 Measurements List for Seroe Domi Formation, Seru Blandan and St. Michielsburg Outcrops 208 209 211 212 213 214 215 216 217 218 219 220 221 222 223 224 225 226 227 228 229 230 E tiff g. 4- E E #142. E 1" ~ . LN . . Wes . \ ' nr . < A 1 , “109. MS ‘ ‘ ‘ " 1 7'3 1 , l .__f ‘ are. . ) ~13 . . A ‘1 ‘ ' " AL ‘ l "» , . - _ ‘ H A I ’ Q ,' . 082 L: ff 7'1", .5: ‘ _ J ‘ , , . V ¢ Lg- *" ' ‘ .4 -' .— 'JX.‘ ‘ ‘ ‘ l w '24 '4': )"z' . 2 ‘1"12 s‘('~v:-' - . r ‘ I"; Y4 , W L :L-n ‘LCN '1 “Srr’tfl , "r 53"“ .:. 4 _ * .1 ' 7* ' .. -- v . I A 1.1! 6"" ’3': 7 .‘04 t I» . ..'. , . .. n: . l. . J ml. . 9% " u ‘45-“:- .. , ‘ ' . - 457 . d: :‘(m "“ .Juf-athv_. ~i ‘ -’ n r: . .‘Jl‘ . .JI‘: u..-» , ‘ ’1'. “ '31”. V ' q x , , W , .a- l ‘ 3_ ‘..‘\ :15: ’ p'?’ I f - "Q «n: . - ‘ . , \ ’ A i l ‘ u ' 1 - l 'v-F; v' — :Aln 114 ,‘ . 4 Li . A" ‘ 7‘4 v' " J-1‘ "1 w. . "" 1m“: ( “ I Table Table Table Table Table Table 88. 89. 90. 91. 92. Sample Sample Sample Sample Sample Sample SB-l SB—l SB-2 SB-2 SM-l SM-l Zone Zone Zone Zone Zone zone I Measurements II Measurements I Measurements II Measurements I Measurements II Measurements 231 232 233 234 235 236 ’Lr'. p 7 q- A l viismevua n .b ,5. , .3. .. A .‘n L‘ .6 M? E\- as Ce £ Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure List of Figures 1. Qualitative Comparisons of Growth Rate(after Sunagawa 1984) 2. Population Trend for Mononuclear Crystal Growth 3. Diffusion Limited Growth Model for a Crystal Through Time 4. Population Trend for Polynuclear, Birth and Spread, Spiral and Diffusion-Limited Growth Models 5. Family of Trends for Mononuclear Crystal Growth 6. Family of Trends for Polynuclear, Birth and Spread, Spiral and Diffusion-Limited Growth Models 7. Cathodoluminescent image of Burlington-Keokuk sample from the Dallas City Quarry. Arrows point to dissolution of dolomite cores (1 inch = 100 microns) 8. Partially crossed polars view of Highway 61 Burlington-Keokuk sample (Missouri). Arrow points to crinoid fossil mold (1 inch = 200 microns) 9. Cathodoluminescent view of Highway 61 Burlington-Keokuk sample. Arrows point to slices of dolomite rhombs that exhibit all the zones encountered (0.75 inch = 100 microns) 10. Burlington-Keokuk Isotope Data, 8WD versus 8BC (after Banner et al. 1988) 11. Cathodoluminescent image of Seroe Domi Generation I dolomite crystals. Arrows point to crystals that exhibit all of the zones encountered (1 inch = 50 microns) xfi 11 28 29 31 33 34 37 39 40 41 44 'v. ..“.,: . '0“I— .. . .. v . A -¢“... I. ‘~._ .— - . 'P -_ A. . ~- .‘ . “_ C. . ‘~ ~ . a f-.‘- Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure 12. Partially-crossed polars View of Seroe Domi 13. 14. 15. 16. 17. 18. 19. 20. unimodal planar dolomite (0.75 inch = 100 microns) 45 Cathodoluminescent image of Seroe Domi sample showing brightly luminescent dolomite generation II replacing generation I dolomite (1 inch = 100 microns) 46 Cathodoluminescent image of Seroe Domi sample exhibiting dissolution of dolomite cores. Arrows point to edge of interior dissolution of generation I dolomite crystals (1 inch = 50 microns) 47 Cathodoluminescent image of Seroe Domi sample exhibiting inclusions and dissolution. Left arrow points to an inclusion. Right arrow points to dissolution (1 inch = 50 microns) 48 Seroe Domi Isotope Data, 6WD versus SEC after Fouke et a1. 1996 51 Cathodoluminescent view of Saluda dolomite crystal. Arrows point to crystals exhibiting all encountered zones (1 inch = 80 microns) 55 Cathodoluminescent view of Whitewater dolomite crystal. Arrow points to crystal exhibiting all encountered zones (1 inch = 100 microns) 56 Saluda and Whitewater Isotope Data Smo versus Plain light view of Saluda mudstone. Arrows point to top and bottom of lamination (1 inch = 200 microns) 6O Partially crossed polars view of Whitewater peloidal grainstone. Arrow points to relict outline of peloid (1 inch = 100 microns) 61 Plain light view of Whitewater peloidal grainstone. Dolomite rhomb (indicated by arrow) is replacing compacted ostracodes ( 1 inch = 100 microns) 62 fifi --~ '9 Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure 23. 24. 25. 26. 27. 28. 29. 30. 31. 32. 33. 35. Closeup view of dolomite rhomb in Figure 22 ( 1 inch = 50 microns) 63 Plain light view of Whitewater peloidal grainstone. Arrow points to dolomite rhomb replacing an ostracode (1 inch = 200 microns) 64 Partially crossed polars view of Saluda packstone. Arrow points to fossil fragment ( 1 inch = 200 microns) 65 Partially crossed polars view of Saluda packstone. Arrow points to fossil fragment ( 1 inch = 200 microns) 66 Partially crossed polars view of Saluda wackestone. Arrows point to crinoid fragments ( 1 inch = 200 microns) 67 Partially crossed polars view of Saluda wackestone. {Arrow points to crinoid fragment (1 inch = 200 microns) 68 Partially crossed polars view of Saluda wackestone. .Arrow points to crinoid fragment (1 inch = 200 microns) 69 Partially crossed polars view of Saluda wackestone. Arrow points to bryozoan fragment (1 inch = 200 microns) 7O Isotope Data, Smo versus SBC 72 Location Map 74 Highway 421 Outcrop of Saluda and Whitewater Formations. Arrow points to coral layer at base of Saluda 75 Highway 7 Outcrop of Saluda and Whitewater Formations. Arrow points to coral layer at base of Saluda 76 Highway 56 Outcrop of Saluda and Whitewater Formations. Arrow points to coral layer at base of Saluda 77 xw Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure 36. 37. 38. 39. 40. 41. 42. 43. 44. 45. 46. 47. 48. 49. 50. 51. 52. 53. Highway 61 outcrop of Burlington—Keokuk Formation 78 Seroe Domi, Seru Blandan and St. Michielsburg Outcrops, Curacao (after Fouke et al. 1996 and Fouke unpublished field notes) 79 Saluda Hwy 421 Outcrop Profile 81 Saluda Hwy 7 Outcrop Profile 82 Saluda Hwy 56 Outcrop Profiles 83 Burlington—Keokuk Hwy 61 Outcrop Profile 84 Zone measurements of rhombic slice (shaded band represents zone measured) 85 Comparison of length measurements between two observers 87 Comparison of replicate analyses for first observer 88 Comparison of replicate analyses for second observer 89 Saluda/Whitewater Formation crystal size frequency 93 Burlington-Keokuk Formation crystal size frequency 94 Seroe Domi Formation zone I crystal size frequency 95 Seroe Domi Formation zone 11 crystal size frequency 96 Saluda Mudstone (sample M20) 103 Saluda Grainstone (sample G8) 104 Saluda Packstone (sample A5g) 105 Saluda Wackestone (sample Pay 5) 106 I v, .. My. mu..- -_—"'* Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Figure Seroe Domi Dolomite, Seroe Domi Dolomite, sample. crystals Keokuk sample. Crystal A Crystal B Slice Measurements Case II Solution Case I Solution Triangle A’B’C’ Saluda Interbedded Mudstone Whitewater Peloidal Grainstone Burlington-Keokuk Crinoidal Wackestone (sample DFS 24) Zone 1 Zone II Cathodoluminescent view of Saluda dolomite Arrows point to adjacent (1 inch = 100 microns) Saluda Paired Crystals Burlington-Keokuk Paired Crystals Partially crossed polars view of Burlington— Arrows point to large crystals near pore and within matrix 100 microns) Family of functions for dr/dt Three cases of rotation with corrections (sample D12) (sample P 27) (sample SB1) (sample 881) (paired) (1 inch 107 108 109 110 111 115 117 118 122 128 129 133 137 138 141 142 144 . a, c” ‘ l .! .Q. I INTRODUCTION Carbonate reservoirs are conservatively estimated to contain approximately 60 percent of recoverable oil globally (Roehl and Choquette 1985). Carbonate rocks also cover approximately 10% of the continents (Ehlers and Blatt 1982) and serve as productive aquifers in the subsurface (Domenico and Schwartz 1990). As a result, much effort has been devoted to the study of carbonate precipitation (Berner 1982, Lasaga 1981, Land 1980, Berner and Morse 1974). Carbonate precipitation and dissolution have been studied in every environment ranging from the surface to deep subsurface (Lucia and Major 1994, Negra at al. 1994, Purser et al. 1994, Feazel and Schatzinger 1985, Harris et al. 1985, Sandberg 1985, Walter 1985, Choquette and Steinen 1980, Mattes and Mountjoy 1980). In particular, much attention has been paid to dolomitization because of 1) the abundance of dolomite in the rock record compared to the modern day and 2) the reservoir potential of dolomite (Nordeng and Sibley 1996, Sibley et al. 1994, Sibley 1980). The dolomitization reaction has been investigated extensively both from a microscopic and a macroscopic viewpoint resulting in identification of kinetic catalysts and inhibitors as well as formation-scale dolomitization models (Morrow and Abercrombie 1994, Nordeng and Sibley 1994, Sibley et al. 1994, Simo et al. 1994, Usdowski 1994, I « ..|F|ll\l . . . . -ll...| . L L. .. .. . _. v3 . . a. . Io.... . u. L. l. i. .1 . _. o - so . o l . . ... .n. .. Vs ... Va . . A. ‘. I . 5. s. ‘- AL. ...\ ... ... 4. . . . . . .. .A o . . . . v. 1. flu . .. . . T~ fix . .n u.. . ... ... u. .. . . . \. . .x 6. us. . vs . a «.4 . w »\ .14 s. s-H . . _ . o v . ..o . . .o ..o . .b ... . . ... .-I. ..l. u . .n. . . n . . . y .. .\ \ L. .. _ ... . .. .. .,. . . 1!. .u. . ... a. . . .u. i. . . us. «. 2. N. T» .a. . v .. «L... O t \l - Vahrenkamp and Swart 1994, Whitaker et al. 1994, Fouke and Reeder 1992, Middleburg et al. 1990, Sibley 1990, Sibley et al. 1987, Sibley and Bartlett 1987, Bullen and Sibley 1984, Gregg and Sibley 1984, Saller 1984, Sibley 1982, Baker and Kastner 1981, McKenzie 1981, Carpenter 1980, Choquette and Steinen 1980, Gaines 1980, Land 1980, Lumsden and Chimahusky 1980, Muir et al. 1980, Zenger and Dunham 1980, Katz and Matthews 1977, Badiozamani 1973). However, very little is known about the mechanism of dolomite crystal growth because of two factors: 1) the lack of a modern analog for massive ancient dolomites, and 2) the inability to precipitate dolomite at standard temperature and pressures in the laboratory. The latter obstacle has been overcome by extrapolating high—temperature, laboratory crystal growth experiments to lower temperatures. From these experiments in dolomitization, researchers have found: 1) an induction period for dolomite precipitating on a calcite, aragonite or dolomite substrate (Sibley et al. 1994, Gaines 1980, Katz and Matthews 1977), 2) an increase in the rate of dolomitization with increasing temperature, surface area of substrate, and Mg/Ca ratio of solution (Sibley 1990, Sibley and Bartlett 1987, Katz and Matthews 1977), 3) a faster rate of reaction when aragonite is used as the substrate as opposed to calcite (Katz and Matthews 1977), and 4) a decrease in the rate of dolomitization with the addition of sulfate to solution (Baker and Kastner 1981). However, these experiments have not demonstrated whether the growth mechanism is a diffusion-limited or surface reaction-limited process. Diffusion of C05‘ ions or diffusion of dehydrated Mg2+ are possibilities for a rate-limiting step. A surface reaction-limited process is also feasible. The progression from a less than 50% molar Mg dolomite to a stoichiometric (50% molar Mg dolomite) allows for a change in surface free energy and a possible change in available nucleation sites. SEM images of partially dolomitized calcite show dolomite preferentially grows at substrate edges and corners (Kessels 1995 Figure 6, Sibley et al. 1987) suggesting either: 1) a higher concentration of COf‘ ions as a result of faster dissolution of calcite corners or 2) the development of favorable kink sites for nucleation and/or layer growth at the dissolving calcite edges. Thus, the question of diffusion-limited versus surface reaction-limited growth cannot be answered by ex situ observations. Kessels (1995) also indicates surface topographies consistent with a two—dimensional nucleation and layer growth mechanism. However, two-dimensional nucleation and layer growth can occur in both the diffusion- 1imited and surface reaction-limited growth cases since the method of attachment in diffusion-limited growth is independent of the rate—limiting step. Recent methods of dolomite crystal growth mechanism determination include dolomite crystal size distributions on. ‘1- and cathodoluminscent zone-width vs. crystal-radius plots (Eberl et al. 1998, Nordeng and Sibley 1996, Sibley 1980). Eberl et al. (1998) generated crystal size distributions by successive iterations of known crystal growth models and then uses the crystal size distributions generated as a standard for each model. Thus, the crystal size distributions of actual crystal data can be compared to the model distributions and used as an indirect means to determine crystal growth mechanism of natural crystals. There are three assumptions that are necessary to use crystal size distributions to determine crystal growth mechanism: 1) the crystal growth mechanism does not change at any time during precipitation, 2) crystals do not nucleate at different times, and 3) no one crystal precipitates for a longer period of time than any other crystal. The extent to which any crystal size distribution is a determinant of crystal growth mechanism depends on the validity of these three assumptions. A second approach is the measurement of zones as an estimate of growth rate (Carlson 1989, Kretz 1974, 1973). Kretz (1974, 1973) and Carlson (1989) investigated the growth of garnet crystals by examining compositional zones. Kretz (1974) considered growth rate as a change in radius, dR/dt=k, volume, dV/dt=k, and surface area, dA/dt=k. Carlson (1989) plotted the normalized radius versus the normalized rate for garnet crystal measurements. The . , .. _ e . . 2. .. _ . . . , .. . _ L. _ l. .: z. .3 l. .. _._ A. L.- ... Q» n\. ». a: .‘ a. v. t. . . . . v. . . .1u :. a: , . . e _ a ,5 44 6 ~ »~ . r: e . .u t. . a. u. r . . e “I. .3 u. me p . G. . .u. .u . .. .1. v? .u. :. 4a a. .. en .1 .. rs . e . \ x .1 .—. .. .. .. .. y. .. p. w .. G. .. y. .. 8.. .. .. .9 2 . .. .» . .. >~ .. e. .. 2 C. -. 6. v. e S .«u a: . measurement technique outlined in Kretz (1973, 1974) uses the radial distance between any two compositional contour lines as the rate and the distance from the center of the crystal to the midway-point between the compositional contours as the radius. Kretz (1974) and Carlson (1989) both found actual measurements of garnet zones versus garnet crystal radius did not fit any of the three models (see Figure 3, Carlson 1989). Kretz (1974, 1973) identifies changing rates of nucleation as a possible problem for the models. Like Kretz (1974), Carlson (1989) attributes the trend to changes in nucleation rate caused by the increase in temperature (thermally-accelerated nucleation). Nordeng and Sibley (1996) followed a similar procedure using cathodoluminescence zones. Data for individual thin sections could be fit with a straight line, dr/dt=kr, where growth rate increased with crystal size, that also did not fit any of the known growth models. Nordeng and Sibley (1996) interpreted the size dependency of growth rate to thin section-scale, solute flux-limited growth. Crystal zone data and crystal size distribution data for dolomite have been interpreted as an indicator of a solute—flux limited reaction (Eberl et al. 1998, Nordeng and Sibley 1996). This interpretation would suggest the dolomite growth rate of adjacent lithofacies exposed to the same dolomitizing fluid will vary with lithofacies type, or changes in porosity and permeability, that affect solute t O" 69?“'~‘~~O ' "H ' .. .1. .fi .\ C u I u r... .nu .!A .~‘ FL. .p. r§ .ks .n< .: u. .u. a . . s v. P s . e . 5.. ‘k. ‘ . .xs .II. x \ an. . ‘ nx» A . I .q. ..a. ~ ~ .5. . ‘ ..... ... 7. uk- v~ v D. . In. a - Q\~ . flux. Thus, a lithofacies with an initially high permeability would undergo a faster rate of dolomite growth than adjacent lithofacies with initially low permeability. Consequently, in open and closed systems, porous lithofacies would grow faster than adjacent less porous lithofacies until the porosity of the adjacent, initially less—porous lithofacies, was reached. This evolution toward "porosity equilibrium" is one possible explanation for the consistency of dolomite rock textures. In order to determine the variation in crystal growth mechanism spatially, cathodoluminscent zones widths and crystal radii are determined for samples from a regularly spaced grid. A body of rock that does not have a variable crystal growth rate mechanism can be described as a unit of rock in which: 1) the net rock-water interaction is precipitation and 2) the rate—limiting step in precipitation is the same throughout the unit of rock. Net rock-water interactions that add to a crystal are based on the amount of influence exerted by two processes in crystal growth; solute flux and solute uptake. Solute flux to a growing crystal surface in a formation is influenced by the amount of interface between crystal surface and solution (pore size) and transportation of solute to the crystal surface (hydraulic potential, pore geometry and interconnectivity). The latter affects the concentration of solute in the bulk solution that in turn affects the concentration and .1" ..—-—-~ ‘ (9'1 1 ._ . .. .. .. ._ ... . e. . as L. ac :f o. .H. . L. .. ._. .g L. o. s Na. K s s e ‘ 5.. . v. _. «a .x» .0 ‘. vs a — . .* pk» \ .. n 5.. . .... v . ... . . . . L. . u. ... a \ . . C. Le «\w ... .1.» .: ... .o. o . . . v. ._. 7. .~. . a . . . u . . e x .x. .1. I. I I. . . ~. .~ .. v. . I. . .. a .. .. ‘ >4 x . A s\\ L. thickness of the interfacial solution. The interfacial solution is the fluid that is bound to the crystal surface where dangling ions and surface charge attract Hg)rmnxa strongly than surrounding molecules of H53 in solution. The tendency for ions to attach and detach from the surface of a crystal is a result of the drive to maintain equilibrium between the interfacial solution and crystal surface. Precipitation results when the net ion surface exchange represents solute uptake. The rate-limiting step in crystal growth can be dominated by either of the two processes, solute flux or solute uptake. For solute-flux limited growth, the rate- limiting step is delivery of ions to the surface. For an individual crystal in a stagnant solvent, this process is known as the diffusion limited growth model (Table l) and the gradient in solute concentration projecting outward from the crystal surface results from the growth of the crystal itself. For a population of crystals growing by solute-flux limited growth, variation of the solute concentration may result from: 1) interaction of crystals with solution or 2) changes in the external source of the solution. Mixing of two fluids, meteoric and marine, or introduction of an entirely new fluid would represent an external source for solute variation. On the scale of a crystal, when the rate-limiting step is attachment of ions to the surface, the process is referred to as surface-reaction limited growth. 7...... :41 .......\ £121... Atty: . .....T..>. c.3151 .Ifitafi. \ TQ SC»... .3...£\........\\ 1...“... , ‘ 2'1...) ...3...._ _....:..... T; ...:...._..:?; 1...... £252... :.:...1 .\ 232...... mSHomu Hmummuu ma 9 snow Hmumwuo cam conSMMHU muSHom .coflpmuucwocoo COHDSHom mcflucmwmuaou ucmumcoo m me x o x u uc\up HI no u\x u poxuo nuzouw omouam cam nuuflm mommn5m :o oxmums ace 0 x u uo\up nuzonm Hmuflmm momqum co oxmuas QOH o x u uc\uo nuzouw ummHosamaom momMHSm so oxmumd aoH N wax u uo\up zuzono ummaoscocoz wUMHHSm Go mxmum: GOA an u\x u uc\up zuzouw omuflfifiq coflmsuuflo oommudm on mnm>flamo Goa H CH cowumzom mzubwa meow ocwmeDE Hmpuo cowuomom cuaonw amumxuu Hmbpz.auzoum amumhuu How noum ocwuwswq mumm suzouw Hmummuu wow mcoflpmsvm mumm nuzouw Hafiomm .H magma For a population of crystals, the process will be referred to as solute-uptake limited growth. Previous surface-reaction limited mechanisms which have been proposed and mathematically modeled for the different styles of ion attachment to theoretical crystal surfaces include: 1) mononuclear growth, 2) birth and spread growth, 3) polynuclear growth and 4) spiral growth (Christian 1975, Ohara and Reid 1973, Nielsen 1964, Burton et a1. 1951). A crystal growing by any one mechanism will fit the crystal growth rate equation: dr/dt = f(x) = kznrn where f(x) is a function of crystal size, r, or a constant, k, depending on the model type (Table 1, see Reaction Rate section for a detailed description of each model). Thus, a unit of rock could be described by one mechanism if the growth of the crystals in that unit of rock can be described by the same crystal growth rate equation. The intention of this study is to determine: 1) the scale of rock units that can be described by one crystal growth mechanism and 2) if rock units characterized by a specific crystal growth mechanism coincide with lithofacies in dolomites. If a single lithofacies can be represented by more than one crystal growth mechanism, then the fluid is exerting a greater control on the rate of precipitation than variation in lithofacies. If different lithologies from the same dolomite share the same crystal growth mechanism, again WWWW .III- -"~ . -‘ ,A “L_ " Id .'. .. .I- C - -~- .-4 p--,.-. o- ..-._ .-.-- ‘-_. a" 1 O n t J l f I!) the fluid exerts a greater control than the variation represented by the different lithologies. If only similar lithofacies from different dolomites share the same crystal growth mechanism then the lithology is exerting a greater control on the rate of precipitation than variation in the dolomitizing fluids. If different lithologies from different dolomites have the same crystal growth mechanism then the mechanism is: 1) independent of the lithology variation represented by the rock types compared and 2) operating over a range of fluid compositions as represented by the variation in dolomitizing fluids. Reaction.Rate The rate of crystal growth is related to crystal growth mechanism (Sunagawa 1982). Mononuclear (dr/dt =kr2), birth and spread (dr/dt=k/r or dr/dt=k), and polynuclear (dr/dt=k) growth mechanisms represent a spectrum of growth mechanisms in which nucleation rate is increasing (Figure 1). The increase in nucleation rate leads to an increase in growth _rate. Spiral growth, which is represented by dr/dt=k is independent of crystal size and nucleation rate (Burton et al. 1951). Nielson (1964) proposed the equation dr/dt=k/r for a combination of mononuclear and polynuclear growth based on the results of a probabilistic model. The equation dr/dt = k/r is a result of polynuclear growth occurring 60% of the time and mononuclear growth occurring 40% of the time 10 c u a ' 0 DO . fl . 1 h a. Q . '9 cuzouo umoaosc>aom omuaafla cofluomou momuudm cuzoum Umoudm cam sweep pouflafla coauomou oomwusm cuzouo ummHoscocoE cmuflefla cofluomou momMHSm wumu coflummaosc [solute] Qualitative Comparisons of Growth Rate Figure 1. (after Sunagawa 1984) 11 ||rllu - u. _o . o . . s u .. . ~ . a 9. w .. .. L... .3 v . 73 4. r .. ..fi ». “A. e. .2 N. .3 ... a. .2 . ~ .2 e. vs a .. .. . _. a . __ u. L. . . ~ .. 7.. x. a. L. L. . Q. . a a. >.. .: a. . r. .1 .m .. .. _ A . . . .C ... \N . . a. p. e e. .2 {a v. _ .. L. .. ... _. T. L. .. . ... p. a. ‘g L. a; 2-. u... >. is . . v. p“ -. .. . . . I. . .. .. I. .. v. u .. .. .. ‘ . .. L. b. 2. — . . a. .. .1. . . a; .. ~.u ... g . o . ... . . a . . . .s a . . .s» .‘v u \ s. «x. \xi 6 .. '.".‘.Ip.;.:,(.!g‘.l|_[u-,_...-§o"vto . during any time period of growth. Ohara and Reid (1973) combined the physical models of mononuclear and polynuclear growth to define the birth and spread model, dr/dt = k. In the latter version of the model, a layer is always generated by more than one nucleus and layer growth between the nuclei occurs at a finite rate. In review of the models, Nyvlt (1985) also indicates the equation for birth and spread should be independent of radius based on the physical assumptions behind the birth and spread growth mechanism. The two assumptions are: 1) nuclei can form anywhere and 2) the growth rate of faces is constant (Nyvlt 1985). If the assumption of a constant nucleation rate per unit area per unit time is true, then the rate of radial growth of a crystal growing by birth and spread growth is only dependent on factors affecting nucleation rate. By allowing nuclei to form anywhere on the surface and allowing more than one nucleus to form at a time, growth is independent of crystal size. This is in contrast to the mononuclear growth model where each layer grows laterally away from only one nucleus resulting in growth dependent on the surface area of the crystal. Diffusion-limited growth (dr/dt=k/r) is treated separately since the way in which the ions attach to the surface is not the rate—limiting step. Fewer ions approach the crystal surface per unit time in diffusion-limited growth than necessary for any of the surface reaction 12 limited growth models under the same conditions. Consequently, diffusion-limited growth has the slowest growth rate when comparing growth rates of any one mineral. The growth rate in the spiral growth (dr/dt =k) model, which is independent of nucleation rate, cannot be compared qualitatively to the other growth models. For each of the different crystal growth mechanisms, relationships between growth rate and crystal size can be derived from the crystal growth equations and assumptions about ion attachment. By integrating the three crystal growth equations over one increment of growth, three crystal population trends emerge: l) zw=[kTrf/(l-kTr1)], the population trend for mononuclear growth, 2) zw=kT, the population trend for polynuclear growth, birth and spread growth, and spiral growth, and 3) (zw)2+2(zw)r¢ = 2kT, population trend for diffusion-limited growth (Table 2) (the latter growth model trend will be rejected in favor of zw=kT, see discussion in Population Trends for Crystal Growth Mechanisms section). In the population trend equations, zw is the increment of precipitate added to the surface (or rynn), r1 is the crystal size before the increment began precipitating, rzis the crystal size after the increment finished precipitating, T is the time interval over which precipitation occurred, and k represents solution and growth conditions. The increment of precipitation or 13 Table 2. Summary of relationship between crystal size and increment of new precipitate Mononuclear Growth Spiral Growth Any mechanism of ion and attachment Polynuclear Growth surface-reaction- surface— diffusion-limited limited growth reaction- growth limited growth dr/dt=kr2 dr/dt=k dr/dt=k/r dr(1/r2)=kdt dr=kdt rdr= kdt r-Zdr=kdt r2 t2 r2 t2 .2 t2 Idr=kjdt Irdr= kIdt Ir_2dr = k] dt ‘1 H II t1 1:1 1:1 r2‘r1=k(t2't1) let T =t2-t1 1/2 (r22'r12)=k(t2_t1) (l/r1)-(l/r2)=k(t2-t1) rz-r1=kT let T =t2't1 r22-r12 = ZkT let T =t2-t1 (l/r1)-(1/r2)=kT zw=[kTrf/(l-kTr1)]* zw=kT * (zw)z+2(zw)r1=2kT * * zw is the width of the next increment of precipitate added, or r2-r1. k is a constant representing solution concentration, diffusion and crystal form. r1 is the crystal radius before precipitation of the zone. rzis the crystal radius after precipitation of the zone. solute ‘ " § ~ . .2 . .~ . . c c b s O v «xx . g .. ~.. t. ~ v . I O n A I. . . . .. T; L. «4. .2 C. a; .s s bx : d . ‘ a . D s pn. b \ fi— DK - b .. .— n n N . ~s- As» «\s I w. .nfl zone width (zw) can represent luminescent zones or other nonluminescent compositional zones. As ions approach the crystal surface, each event can be described as: 1) ions contact the crystal surface and "bounce back" away from the surface, 2) ions contact the crystal surface and "stick", 3) ions contact the surface and then migrate laterally across the surface, or 4) an ion collides with another ion in solution or another ion migrating along the surface of the crystal. In the latter event, the ions may adhere to each other and the crystal surface or “bounce” away from each other and disperse either into the solution or across the surface. If the collision results in the ions adhering to the crystal surface, a nucleus is formed. A nucleus is a unit of the new precipitate inferred to have the shape of a half sphere laying on the crystal surface. The shape is deduced from surface area to volume ratios. A half sphere is the most energetically stable configuration ions could form on the surface. Ions that contact and adhere to the exposed nucleus form a layer of precipitate, which spreads laterally across the surface. This process is referred to as layer growth. Crystal growth mechanisms have been modeled with relative rates of nucleation and lateral growth. In diffusion-limited growth, the relative rates of nucleation and layer growth across the crystal face vary as a result of 15 .' _ \ W a L» n N. s» L. . r . .A. vs .. . u. .. w ..~l.. s ‘ Vuwx— variable solute concentrations. Since the diffusion of ions to the surface is the rate-limiting step and the size of the diffusive layer surrounding the crystal increases as the crystal grows, the overall rate of crystal growth is inversely proportional to crystal size. As the crystal grows larger, it will grow more slowly since it has grown by diffusion-limited growth longer and has created a larger diffusion-depleted “halo”. Thus, as an individual crystal grows, the rate of nucleation and layer growth decreases proportionately to its size. Mononuclear crystal growth is dominated by lateral growth in each growth layer. The rate of lateral layer growth is much greater than the rate of nucleation. Thus, an individual nucleus spreads laterally across the surface before another nucleus forms. The formation of a nucleus is the rate-limiting step. Polynuclear crystal growth is the other end member of the spectrum between mononuclear and polynuclear growth. In the polynuclear case, the rate of nuclei formation greatly exceeds the rate of lateral growth. In Nielson's version (1964) of polynuclear growth, there is minimal lateral growth occurring as nuclei intergrow at a finite rate. In Ohara and Reid's version (1973) there is zero lateral growth occurring between nuclei. Using either version, individual monolayers form almost entirely by accretion of nuclei rather than lateral growth. Both versions of polynuclear growth lead to dr/dt = k. Thus, the boundary between 16 '.- 6‘. _g' fi‘y‘ “' an h ‘.1 'F—F - t-v-n "' ‘F‘ I ' r. _.. A». mononuclear and polynuclear growth is defined by the number of nuclei. In mononuclear growth, one nucleus gives rise to one growth layer (one d-spacing high or greater) and the time between individual nucleation events may be very long. In polynuclear growth, a single growth layer (one d-spacing high or greater) forms by accretion of nuclei on the surface. The intermediate case between mononuclear and polynuclear growth is described by a separate growth model referred to as birth and spread growth. In the birth and spread growth model, more than one nucleus forms per growth layer but lateral growth still occurs. As discussed previously, birth and spread growth has been tentatively represented by dr/dt = k/r and dr/dt = k. Nielson’s model (1964) combining mononuclear and polynuclear growth resulted in dr/dt = k/r. In that study, a probabilistic model was used in which the average time for completion of a growth layer was defined as: I =‘n_ + 0.6 12 (page 50, Nielson 1964) where Ilis the time between successive nucleation events and ‘Q is the time required to form a complete growth layer. In order to express the equation in terms of growth, Ilis substituted with the mononuclear growth equation and‘b is substituted with the polynuclear growth equation to result in dr/dt = k/r. While the analysis is straightforward, Nielson warns “such detailed conclusions are not justified 17 . . . . I .. . v. .H .. .. . . . I —. a . . . k ‘ \\ u . n . ‘ . .._ .—. a I p. o. _. rs. . .1. v a ._ >. Fk. . .u . .. I. . . ._. AC g. .. ‘. .r. L. .. .‘ a. .3 .. s; ~... . ... .g L. S. t. .. v. o L. .2 .3 s: .... . ‘ ~ ‘ .2 .. .. . . ,2 .. .. .. .. L. x. v. _C. .0. .. . ... w: . ‘ \. ..-. a. Q. ._. o. ._. _. ‘.. ... ... ., . ... .. a .g. .-_ 5.. . ~ ‘ —- .\» ux ‘ 5‘ .. l. ... ... ‘7. ... . ‘. I. s . L. us 2— : v. .k. I. .h. ~« \~ .... .: 0'; V because so many approximations have been made in order to arrive at this point.” (page 52, Nielson, 1964). Ohara and Reid (1973) combined the ideas of mononuclear and polynuclear growth to arrive at birth and spread growth. Again, in this model there is no intergrowth between nuclei. Each nucleus is modeled as if it will grow to the edge unobstructed. The other two critical assumptions of this model are: 1) lateral growth is constant regardless of the size of the layer growing and 2) nuclei can form anywhere. These assumptions result in the equation dr/dt = k for birth and spread growth. While no definitive equation exists for birth and spread growth, the analysis in this study will approximate birth and spread growth with the equation dr/dt = k. This choice is based on the argument the nucleation rate per unit area per unit time is constant. Another equation has been tentatively proposed by Nordeng and Sibley (1996) from empirical evidence. Nordeng and Sibley (1996) suggest dr/dt = kr may represent a hybrid mononuclear- polynuclear crystal growth mechanism. This equation is also declined in favor of dr/dt = k. If each square unit of crystal surface has the same random chance of forming a nucleus on the surface, then the nucleation rate per unit area per unit time will not vary with crystal size. Thus, crystal size, given the model's assumptions is best described by dr/dt = k. 18 A growth model, which is not constrained by relative nucleation rates, is the Spiral Growth Model (Burton et al. 1951). The spiral growth model describes layer growth away from the crystal face expression of a slip plane. Since portions of the slip plane rise to different heights above the crystal face, adding ions to the leading edge (created by a slip plane) perpetuates the edge of the growth layer through time. This eliminates the need for nucleation, implying spiral growth can occur at saturations below the saturation state necessary for the formation of stable nuclei. Factors such as solution composition, solute diffusion and crystal form affect nucleation and layer growth by changing surface free energy and free energy of formation of the new precipitate (Steefel and Van Cappellen 1990, Nielson 1964). The radial growth rate, dr/dt = k, for polynuclear growth is independent of the radius which intuitively follows from the fact layer growth is an absent to minor component in polynuclear growth. Spiral growth, like polynuclear growth, is also independent of radius. The spiral growth and polynuclear growth rates are both approximated by k (Nielsen 1964). In polynuclear and spiral growth the number of available sites to add an ion to the crystal surface are not constrained by the radius of the crystal when evaluating an individual crystal. Polynuclear growth involves multiple layers precipitating at one time. 19 Spiral growth involves addition of ions along turns of a spiral defect. Thus, the growth rate of polynuclear and spiral growth are controlled respectively by the factors influencing the nucleation of simultaneous layers on a growth surface and the distance between adjacent turns of a spiral or collectively by k. Unlike spiral and polynuclear growth, mononuclear growth is a function of radius as well as k for an individual crystal. In mononuclear growth, the number of available sites is proportional to crystal size since only one layer grows across the surface at any point in time and the overall radial growth is limited by nucleation of the next layer. Thus, the larger the crystal, the greater the likelihood of a successful collision resulting in the formation of a nucleus. In birth and spread growth, nuclei may form on any size layer. Thus, there is more than one available nucleation site utilized per growth layer similar to the polynuclear case. Likewise, birth and spread growth is also independent of crystal size since the number of layers formed per unit area per unit time will not vary with crystal size. crystal Grovth.Mbchanisms in natural Systems The determination of the mechanism and rate of crystal growth has included the use of many different techniques with unique approaches. Previous studies of carbonates used methods including but not limited to petrography, bulk 20 -O' ‘0‘.--- v. .. “ .—. r. . .f ___ c s. .; . ___ _._ .0. Q. ..\ 1 2. cu. . . .. v. .1. .fi— 0 . § ~ who A v~ . ' by. v‘ \H‘ ud ha x 5‘ .r.‘ r. .h» a.» A» ‘ ... 2. a . an. .3 a . .. ... . .. .u .u v. . . _ . . ,ts . a s . -s. .- t; Q I ¥‘ \ . . . L. L a T» » .... .Q a . s . .r.. . . i. . a .. a b x s .. w. as t» p». a. chemical analysis, weight of precipitate, crystal size distributions, cathodoluminscence zone data and crystal and fluid composition from crystals grown at different temperatures and solution compositions in the laboratory (Eberl et al. 1998, Nordeng and Sibley 1996, Nordeng and Sibley 1994, Sibley et al. 1994, Sibley and Bartlett 1987, Sibley et al. 1987, Bullen and Sibley 1984, Gregg and Sibley 1984, Saller 1984 , Carlson 1983, Morse 1983, Sibley 1982, Carlson and Rosenfeld 1981, McKenzie 1981, Reddy et al. 1981, Choquette and Steinen 1980, Gaines 1980). Field approaches included measuring the extent and abundance of dolomite from outcrop and thin sections (Wilkinson et al. 1996, Sibley 1980). Sibley (1980) found dolomite often has sharp boundaries between dolomite and limestone. He interprets the sharp contact as representing the extent that the dolomitizing solution was in contact with the limestone precursor for a time longer than the induction period of dolomite. Limestone in contact with the dolomitizing solution for any period shorter than the induction period would not begin dolomitization. A more recent method applied to crystal growth determination is the in situ analysis of growing crystals with scanning force microscopy. This tool has provided substantial evidence for the growth models originally proposed by Nielsen (1964), Ohara and Reid (1973) and Burton et al. (1951). However, this particular method is best used 21 .11.- .. 1 . < .5. v 1 o .. .1 \. . .. . . .. .. .. .1 .. . .2 L. .. ... .. . L. .. .t. .. _T v. .. ... u. I. .a. H. ‘ . ‘ :. L. L. . ‘ .s. t. 1. .11 I n F... .\ p. m. . .. .. ._ a. _‘ . ;. ~. .~. .. L. \ ... .2 ~. \ .. 5. ~ >\ . .\ .s‘ .n— ~.. .C. . . a. .5. for in situ analysis or ex situ analysis for differentiation between different surface reaction-limited crystal growth models and not as an ex situ tool to distinguish diffusion— limited growth from surface reaction-limited growth. In situ growth of calcite and gypsum under a controlled fluid composition gives insight into the transition between the different surface reaction-limited mechanisms at different saturations (Stipp et al. 1994, Gratz et al. 1993, Hillner et al. 1992, Rachlin et al. 1992). However, these experiments determine the crystal growth mechanism for laboratory—grown crystals and only the last precipitation event in crystals from naturally occurring rocks. Sample surface alteration in natural rocks can etch this surface, altering growth features. In addition, surface analysis of natural crystals does not indicate if all crystals in a given lithofacies had contact with the last fluid. Cathodoluminescence indicates extent and timing of precipitation from fluids of different Mn and/or Fe compositions. Zonal stratigraphy of an individual luminescent zone appearing in each crystal is used to determine the extent of the rock—water interaction for a particular cathodoluminscent zone. The concentric cathodoluminescent zoning in dolomites can be used to determine the crystal growth mechanism for each internal cathodoluminescent zone (Nordeng and Sibley 1996). 22 ( o a .H‘ In carbonate rocks, cathodoluminescence is caused by Mn (Mn”, bhf+), which is incorporated into the mineral. Ferrous and ferric iron has the opposite effect. Zoned crystals reflect variations in Mn and Fe concentrations in the precipitating solution through time (Machel 1989, 1983, Fairchild 1983, Pierson 1978). When Mn is incorporated into the Mg or Ca sites of dolomite, spectral analysis indicates a shift to longer wavelengths giving a range of colors from green to yellow to dark red depending on the valence state and concentration of the Mn incorporated (Pierson 1981). Pierson (1981) also found Mn concentration of only 100 ppm necessary to induce luminescence and a minimum of 10,000 ppm Fe needed to suppress luminescence. Sharp boundaries found between individual cathodoluminescent zones may result from threshold values for the substitution of Mg by Mn that induces jumps in the spectral shift as a result of changes in bond length (Pierson 1978, 1981). The sharp boundaries and variable luminescent intensity of zonation in carbonates allows measurement of zone widths and correlation of zones within formations. To use a zone width as a measure of the rate of precipitation from a particular solution and the three-dimensional variation in zone width from crystal to crystal as a spatial indicator of changes in the rate of precipitation, the following is required: 1) concentric zones can be correlated from crystal to crystal and 2) individual zones are isochronous. 23 . .. .. I . r... .2 v... .. . ,.,_ a. L .. . 1. . .. . v. :. _._ .. . . .. . .. C .7 3. . . T. t. ..._ .. a. .. ... .. .3 .. ... .2 .. . L. 1. ;.. 2. ... .. ... .. .. .. .5 _ ‘ _. Q. .. N. .7 . .n v. 2. ... ... ... .. ... L. L. ~._ . . L. s.. .6. . s . x Q. .. J. .. .. .. :. .. v. .2 3. .. .2 ... . .. .. _. . .. ... .. .\ . . u a .. .. .‘ .. I. .. .. .1 .. .. .. .. .. .. I. ~. .2 x. .. .. A. T. «. .. 4.. .. s5 The first requirement can be visually checked by inspection of crystals over the sampling interval. Crystals with the same zonal stratigraphy should have: 1) the same number of zones, 2) the same ordering of zones by intensity, and 3) correlated zones with similar intensities. The second assumption of isochronous zones is based on groupings by zonal stratigraphy and nucleation arguments. A group of crystals with the same zonal stratigraphy are assumed to have precipitated from similar solutions. This assumption is similar to assigning the same age to correlated lithofacies. In both cases, the assumption of isochronity can be stated with greater confidence for more closely spaced samples and only inferred for samples further apart. Changes in solution are assumed to have occurred nearly simultaneously (faster than the induction period for dolomite growth on dolomite) over the range of crystals with the same zonal stratigraphy. The latter assumption is based on the idea that an induction period should exist for compositional changes in dolomite. Experiments conducted by Sibley and Bartlet (1987) indicate an induction period for dolomite precipitating on dolomite when dolomite seeds are added as a reactant in the dolomitization process. Changes in solution that change the composition (% Mg) of the dolomite may be one cause for an induction period. However, to date, exact experiments investigating dolomite precipitation on dolomite have not been performed due to the 24 difficulty of assaying the composition of initial, small quantities of precipitate. Combination of'Crystal Growth and Solute Flux If a crystal growth unit is defined as a unit of rock that shares the same crystal growth equation, then a crystal growth unit can be defined theoretically by combining reaction rate with solute flux. Solute flux can be divided into high and low solute flux based on the rate of solute flux compared to the rate of solute uptake by crystal growth. High solute flux is when the rate of solute delivered to the surface is greater than the rate of solute uptake by crystal growth (Surface-Reaction-Limited Crystal Growth). Low solute flux is when the rate of solute delivered to the surface is less than the rate of uptake by crystal growth (Diffusion-Limited Crystal Growth). Since k is a function of solution composition, solute diffusion and crystal form; k will be assumed constant for any one crystal. K will also have a constant value for any lithofacies or portions therein containing a homogeneous solution. Since lithological heterogeneity is a function of scale, any heterogeneous rock unit can be described in terms of its homogeneous parts. Each growth model; diffusion— limited growth, mononuclear growth, birth and spread growth, spiral growth, and polynuclear growth represent their own spectrum of conditions under which that style of growth 25 takes place with threshold values at either end of the spectrum. Thus, a range of k values exist for each growth model (Sunagawa 1984). When k is considered to be roughly approximate to solute concentration, the threshold values become threshold saturation states between the different growth models as represented by vertical lines between growth models in Figure 1. Spiral growth can occur over the entire range of saturation represented in Figure 1 because it is independent of nucleation. Defects on the surface of the crystal provide an edge for attachment of ions. As ions attach to this edge, the defect (screw dislocation) propagates through time. The spiral growth rate will also increase with increasing solute concentration but its rate relative to other models is unknown. By integrating the growth rate equations for diffusion- limited crystal growth and the end members of surface- reaction-limited crystal growth from rltx>r¢ and rearranging the equations in terms of r1 and the width of the next increment of precipitate (zone width) yields a function that relates the rate of precipitation to crystal size (Table 2). As stated earlier, in the integrated equations, r1 is the crystal size at the onset of precipitation and r2 is the crystal size at the end of precipitation. Thus ryfln is equal to zone width or the increment of new precipitate added to the crystal surface. 26 :. Pqpulation Trends for crystal Grovth.Mbchanisms In order to determine crystal growth mechanism, plots of ryqn (new precipitate added or zone width) versus r1 (crystal size) for crystal populations can be used (Nordeng and Sibley 1996, Carlson 1989, Kretz 1974). The population trend will reflect the crystal growth equation of the rate- limiting process. The expected trend of zone width vs. crystal size for each of the possible growth mechanisms (Table 2) can be represented by a different family of functions. Mononuclear growth is a complex quadratic equation similar to a parabola except the distance from the vertex increases as distance along the x-axis increases (Figure 2). Rearrangement of the zone width-crystal size population equation for mononuclear growth yields the following equation: r1= (1/k) - (r12/ZW) A plot of (rf/zw) vs. r1 will yield a slope of —1. Thus, a linear fit to the modified mononuclear plot describes how well a data set fits mononuclear growth. Diffusion-limited growth is an inverted hyperbolic function that asymptotically approaches zero (Figure 3). The relationship between zone width, or the thickness of new precipitate added to the surface, and r1, crystal size, is a function of time and increasing boundary layer thickness per unit time for that particular crystal. The equation does not describe a population of crystals because it does not describe any 27 _agogn 0o. tfo:.‘oft¢‘.l. h. , 1.1. ,l'.: "1" o. a o. O. .‘ O, I 0, fl 0 .. o ‘ ' L 9 ( a n or auzouw Hmum>uo umwaoscocoz now ozone coflumHsmom .N wusoflm mmflm Hmum>uo vs N. or o o v N o L. i w . . . i o O. ‘o o fit“.‘ :mo ‘\\V %. ‘ 0.0 z ‘ O u ‘. ;m;xa 0 ss m. w. o u (a o O :mN n 28 ‘ o 1 O. \ O 9’90.- 9"}. 00'. 9Q “'fgvtvtt‘ mane gasonaa Hmnmsno m you Hmuoz gnzono umnflaflq nonmSMMHo .m museum ouflm Hmummuo m” “M mu .N m. p h b b 1 d 1» d or 4 00 di- iro vow 5. NF or qquM auoz 29 _ v. p” r. . . : . . . .L o. .. ‘4 v“ ‘ .3 .v.. r, ‘7 «s» . . ~. ... ... .2 .. v. .. a . .. . um .'. o .p.. u.. a. I: A.» _.. .3 .H .. .. . .. s C. .n A .1 .. .7 . . u. L. a . .. E . \ L .. c . L. .2 .. o .. ._. n. . . r, ._ v. .. ‘. v. s. ‘e a. an a. vs s... s. L. .. r. . ... s. A. v. v. v. .. .a .. . .. ... .: .. .. ... ..a ;\ .3 v . . . .. . . . .. .n s . u .. .. ~ .. ~ .. .: v n. o. p ~ 2. «C .s z. x .. s .. s . T». x .. >x. relationship between the initial crystal size and rate of boundary layer formation. If the crystals are precipitating from the same solution on the same substrate, the rate of the formation of boundary layer per unit area per unit time is independent of the initial crystal size when the mechanism switches to diffusion-limited growth. Therefore, dr/dt = k represents diffusion-limited growth as well as polynuclear growth and spiral growth for populations of crystals (Figure 4). In the case of birth and spread growth, a hybrid case between mononuclear and polynuclear growth, a population of crystals would also appear as a straight line, dr/dt = k, on a zone-width vs. crystal-size plot since the zone width, new precipitate added per unit of time (growth rate), does not change with crystal size. In birth and spread growth, two critical assumptions result in a crystal growth equation that is independent of crystal size. The first assumption is that nuclei can form anywhere on the surface (Nyvlt 1985, Ohara and Reid 1973). The second critical assumption is the rate of growth of faces is constant (Nyvlt 1985, Ohara and Reid 1973). Since nucleation is the rate-limiting step and nuclei are assumed to have an equal probability of forming anywhere on the surface, the rate of nuclei formation per unit area per unit time is independent of crystal size. Therefore, nucleation rate would not vary with crystal size even though it does 30 0:O-=‘O‘O'."' g‘.-... -‘9. "pun- ' 0 O . a. c a . 4 9 o . x ‘ | ' O .Q I . r 0 fl 0 v. D '. P b .I u ‘ § . or mamooz £u3ou0 pmuflaflqucoflmsmuflo paw Hmufldm .Ummudm paw nuuflm .ummaosaxaom How pawns coaumH5dom .v ousoflm mNHm amummuo v. a? or o o v a h 1‘ -.I h .. L! r R « 4 a fit- .. .4 0 O. O 3...; i.-- :0 O. i. N? qqptm auoz 31 ~ ~ vary with solute concentration for the birth and spread growth model similar to polynuclear growth. For the two trends (mononuclear growth, Figure 2 and all other growth models, Figure 4), the crystal growth equation represented by the zone-width vs. crystal-radius plots would fit dr/dt = kr2 or dr/dt = k. For mononuclear growth, a series of equations with a variable distance to the vertex would comprise the function family (Figure 5). For polynuclear, birth and spread, diffusion-limited or spiral growth, the series of equations would consist of horizontal lines (Figure 6). If k is spatially heterogeneous, the expected trend would be different equations from one family of functions (one crystal growth mechanism) or multiple families of functions (multiple crystal growth mechanisms). If each mechanism can be represented by a range of k values, or growth conditions, and each mechanism has different k ranges (Sunagawa 1984), then k varies with mechanism as well as within a mechanism. Thus, the magnitude of variation in k, or growth conditions determines whether the trend is: 1) different equations from a family of functions representing one crystal growth mechanism, or 2) different equations from different families of functions representing multiple crystal growth mechanisms. The latter can be tested by comparing crystal growth mechanisms, or different zone ‘width-crystal size trends, dr/dt=k or dr/dt=kr2, spatially. 32 01. .-o”"‘.¢ng-0I @— nuzouw Hmummuo umwaoscocoz How mucouh mo >HHEmm mNHm Hmum>uo .m ousmflm V— N.. 0.. w 0 V O . i . .1 r .1 o x x I 11.1. 1...... I . a . x .\ 55%. t 1. int. x ‘ x‘ ‘Q ,o x. a x ..o _— .q x Q 4 x Q ;or a a i“ «W :u. I C Q ‘ ‘C #3. qiptm auoz 33 mamaoz auzouw amufiaflquaofimswufio acm Hmuflmm .Ummudm pom nunflm .Hmmaosc>aom How mpcmue no >Haamm .o ousmflm mNHm amum>uo or or v. N. o. o v u o i . i J. v .1 k 0 o O 00 ii... ‘0 0. :u I II III. I I. :v 4 41 ii I! II .o x xx iii a! XI :o .09 .NF 1. VP :ow vQF qqptm auoz 34 4.. f». _\~ - .H .3 v. on .. .. .. . A». ~. .9. v _ . a . 3. I w. m . L. Cw .. vi 3 a. x. I. . . r . . H ”1...“... a . a» 2.. a . .2 C. .2 Ce at . at .. 2. 9. .Nu an O. s» u.. .‘ >.. vs .2 Q. .. .rq‘ «F. .K» . u — p H . - _ .v v pk» .. a . . ‘ :. am . . w... ‘2.“ u. . . . g “Au ~ g m \ . ~ .... . .. Z» \I.. .3 . For spatial comparisons involving one crystal growth mechanism, the variation of the basic equation type, dr/dt = k for example, represents variable crystal growth rates from a single crystal growth mechanism. Intuitively, the latter is expected, since each crystal growth mechanism is expected to cover a range of growth conditions (Sunagawa 1984). Geologic setting The Saluda Formation (Ordovician), Whitewater Formation (Ordovician), Burlington—Keokuk Formation (Mississippian) and Seroe Domi Formation (Miocene) exhibit concentric cathodoluminescent zoning with multiple light (Mn) and dark (Fe) zones. Zones can be correlated on the scale of an outcrop for the Burlington—Keokuk and Seroe Domi formations. Zones can be correlated between outcrops for the Saluda and Whitewater Formations. These formations exhibit intact, zoned rhombs with minimal subsequent alteration at one or more outcrops of each formation. Since zone width is used to approximate growth rate, the same zone needs to be measured within each formation. This condition constrains the choice of formations to dolomites with spatially consistent zonal stratigraphy. Burlington-Keokuk Formation The Burlington-Keokuk formation (Mississippian) crops out across northwestern Illinois, southeastern Iowa, and Missouri (Banner et al. 1988). The Burlington-Keokuk is 35 conformably overlain by the Warsaw Shale Formation (Mississippian) and unconformably overlies the Hampton Formation (Mississippian) (Harris 1982). The Burlington- Keokuk consists of shallow marine deposits on an intracratonic shelf, which was subsequently buried by a prograding delta depositing the Warsaw Shale (Lane and DeKeyser 1980). The unit is characterized as dolomitized mudstones and crinoidal wackestones to packstones (Banner et al. 1988, Cander et al. 1988). The Burlington~Keokuk dolomites can be divided into three separate dolomite generations based on zonal stratigraphy: l) a concentrically-zoned rhombic generation (generation I), 2) a brightly-luminescent, rhombic generation, which is not zoned (generation II), and 3) a dark nonluminescent generation (generation III) (Cander et al. 1988). Generation II dolomite replaced generation I, and generation III replaced both generation I and II. Generation I had undergone dissolution at most outcrops of dolomitized Burlington-Keokuk. Samples from the Dallas City Quarry (Illinois) and outcrops in Illinois and Missouri exhibit dissolution and replacement of Generation I to various degrees (Figure 7). The zonal stratigraphy also varies from outcrop to outcrop in detail and number of zones (Cander et al. 1988). The type of dissolution seen in Figure 7 is characteristic of most outcrops to some degree (Cander et al. 1988). A single outcrop in Eastern Missouri 36 .Amcouoflfi OOH u some Hy mwuoo wuflfioaop wo coflusfiommfip ou ucfloa mzouu< .>MHMSO >uflo mmHHmQ may Eouw wHQEMm xsxowxucouocflausm mo womEH namowoafifidaoponumo .b musoflm 37 W Yr: vwv .3 u“ . _ [ll '- ‘ I .o. - .~. . u h. .5; __ an. A—- A. v. ‘4. :4 w.- .~. . .u .3 .. . . . . .2 .. z» r. L. . . . .. . i. 2. ..~ L. .o.. .3 ~.. . o .e» a; Q. . . v. 5‘ y .t z» A \ V V .qn (Highway 61, north of Bowling Green, Missouri) was found that exhibits minimal to no evidence of dissolution of Generation I across the entire outcrop. This outcrop with its intact zones was used for the study. At this particular site, the Burlington-Keokuk consists of a unimodal, planar dolomite with fossil molds and is interpreted as a dolomitized crinoidal wackestone (Figure 8, 9). The isotope values for the concentrically zoned rhombs of generation I indicate a depletion in SUC and Smo relative to expected marine dolomite of Mississippian age (Banner et al. 1988). This was interpreted to represent a meteoric component mixing with seawater after deposition of the Burlington—Keokuk. The variation in SWO without variation in SBC could also result from normal Mississippian marine waters with temperature fluctuations of approximately 20 degrees Celsius (Figure 10) (Tucker and Wright 1990). However, normal Mississippian marine waters are expected to result in dolomite crystals with higher Sr concentration and lower Fe and Mn concentrations than the Burlington-Keokuk generation I dolomite. Generation I has an Fe concentration range of 500 to 3000 ppm (expected marine value, 16 to 57 ppm), a Mn concentration range of 600 to 1100 ppm (expected marine value, 19 to 22 ppm), and a Sr concentration range of 108 to 123 ppm (expected marine value, 150 to >200 ppm) (Banner et al. 1988). The 87Sr/868r 38 .Amcouofla oom n nocfl Hy UHoE aflmmow pflocfiuo ou wucHOQ 30nu¢ .AHHSOmwflzv wHQEmm Msxommlcoumcflausm Hm >m3£mflm wo 3wfl> mumaoa commouo >Hamfluumm .m mucoflm 39 .AmCOHUHE ooa H gocfi m>.ov .ponwucsooco mocoN wzu Ham uflbflgxm “may mbfionn muflfioaoo Mo mwoflam on uqfloa wzouum .mHQEmm Msxooxncoumcflausm Hm mmzngflm mo 3wfl> unmowwcflfidaoponumo .m wusmfim 4o Hvtn"‘t':’("‘9‘91fi.IHJL-é-u 5.0 o .1)- A ‘1‘! A AAJ“ A A‘ l 5‘ l “ L ‘ A ‘ 2v ‘ A U % T .- g‘Ae it 7. m 45 4 <3 ‘2 -1 (i 1 2 (a 00 -2- .4. .6.L 8 18 0 Figure 10. Burlington-Keokuk Isotope Data, 8ND versus SDC (after Banner et al. 1988) 41 '. ’4 .u. . . .U .4 I I O p.. .a. ratio of generation I (0.70757 to 0.70808) is only slightly higher than the expected marine value (0.7076) (Banner et al. 1988). Mixing meteoric water with seawater and precipitating dolomite from a high water/rock ratio would explain: 1) the depletion and range of Smo and SBC, 2) the high concentrations of Fe and Mn relative to seawater, and 3) the depleted Sr concentration and only slightly higher 87Sr/868r ratio (Banner et al. 1988). The latter results from the low concentration of Sr in freshwater and meteoric waters enriched in radiogenic Sr from interaction with the lower Paleozoic rocks of the Transcontinental Arch (Banner et al. 1988). Seroe Domi Formation The Seroe Domi formation represents a foreslope to lagoonal deposit overlying Cretaceous basalts at the Seru Blandan and St. Michielsberg outcrops, Curacao, Netherland Antilles (Miocene). The tops of the inclined beds of the Seroe Domi are partially dolomitized (Fouke et al. 1996, Lucia and Major 1994). Completely dolomitized sections of first generation Seroe Domi dolomite at the Seru Blandan and St. Michielsberg outcrops occur as lenses of dolomite that dip seaward (Fouke et al. 1996, Lucia and Major 1994, Sibley 1980). The Seroe Domi Formation includes foram wackestones, red algal packstones, coralgal grainstones and boundstones (Fouke et al. 1996). Three generations of dolomite have 42 __r—-u=--a—-fiw‘ v. .. _. I. . r. o. .1 4. .1 L. v. .. . .e. p .. n 7. I v III . been recognized in the Seroe Domi outcrops on the island of Curacao: 1) a yellow—orange, concentrically—zoned generation (generation I), 2) an orange-brown generation with sectoral zoning (generation I’), and 3) a dull orange luminescent generation (generation II) (Fouke et al. 1996). All three occur as both cements and replacement of calcium carbonate substrate (Fouke et al. 1996). Generation I dolomite was used for this study because of its zoned, planar rhombs (Figure 11). The yellow-orange concentrically zoned generation I occurs as dolomite lenses near the base of the section (Fouke et al. 1996). Generation 1' which exhibits uniform zones most often occurs as a pore—lining cement and rarely exhibits complete rhombs and exhibits sectoral zoning. Generation II does occur as planar rhombs contains but does not have internal zones. The first generation of dolomite is a unimodal planar dolomite that obliterates the texture of the precursor substrate (Figure 12). The dolomite (generation I) has also being partially replaced by generation II (Figure 13) and has undergone dissolution (Figure 14). The dissolution patterns in Figure 14 are consistent with dissolution of Ca- rich cores and inclusions (Figure 15). Isotope data have been interpreted as a freshwater- marine mixing zone (Fouke et al. 1996, Sibley 1980) and as 43 .Amcouoflfi on n goafl av pwumucsoocm mocoN map mo Haw uflbflaxw umzu mamumxuo ou uQAOQ mzouufi .wamum>uo wuflEoHop H coflumuwcow HEOQ woumm uo wmmfifl udwomwafifidaopozumu .HH wuswflm miov .Amaouofla OOH n noqfl wuHEoHoo HMQMHQ Hmpoaflcs H809 wonwm wo 3ofl> mHMHOQ pwmmouo -maamflnumm .NH mngaflm 45 .AmcouoHE OOH u nocH HO wuHEoHop H coHumuwcwm quomHQmu HH coHumnwcmo muHSoHop ucoomocHEdH >Hu£oHun OcH30£m oHQEmm HSOQ moumm Ho wmmEH unwommcHfidHoposumo .MH musmHm 46 .HmcouoHE om u noaH HV mHmum>uo ouHEoHop H coHumumcwm Ho coHusHomme HOHuwucH Ho mmow ou ucHom m30uu< .mmuoo muHEoHop Ho coHusHomme quuHQanm mHQEmm H800 mouwm Ho mamEH ucmowocHEdHoponumo .vH wHSOHm 47 .AmcouoHE on u nocH HO coHusHomme on mucHom zouum uanm .GOHmsHocH cm on mpsHoa zouum uwmq .coHusHomeo ocm mconsHocH ocHananw oHQEmm HEOQ mouom Ho womEH ucwommcHESHooonpmo .mH wuson 48 “‘5'” I . . Q - .L. hypersaline seawater (Lucia and Major 1994). Evidence in favor of a mixed freshwater—marine interpretation include Smo values that are consistent with normal surface temperatures and SBC variation similar to modern seawater- freshwater mixing environments (Fouke et al. 1996, Machel and Burton 1994, Machel 1989). Evidence in favor of hypersaline seawater dolomitization is based on the geometry of the dolomitized lenses. A zone of undolomitized limestone that should comprise the upper freshwater lens is absent. In addition, dolomitization does not crosscut beds as expected for a mixing lenses moving deeper into the section as regresssion of seawater occurred (Lucia and Major 1994). Evidence against hypersaline seawater dolomitization is that the shape of the dolomitized lenses is a result of dolomite selectivity (Fouke et al. 1996). Fouke et al. (1996) argue that precursor beds for the stratiform dolomite bodies were more readily dolomitized than the surrounding limestone precursor. In addition, concentrations of the trace elements Na, Cl and.SO4‘are lower than expected for a dolomite precipitating from evaporated seawater (Fouke et al. 1996). Further evidence in support of mixed seawater-meteoric dolomitization includes: 1) SBC and SmO values lighter than the estimated marine dolomite and 2) low Mg calcite cements encrusted by generation I dolomite (Fouke et al. 1996). The latter 49 ._. suggests a period of subaerial exposure immediately prior to precipitation of generation I dolomite. The variation in BBC and SmO has also been suggested to represent mixing of marine and freshwater with different total dissolved carbon concentrations and soil-derived C02 (Fouke et al. 1996) (Figure 16). If the two fluids mixing had the same total dissolved carbon concentration, a plot of SWO vs. SUC values would fall on a line with a slope of 1. In this case, the freshwater has a higher total dissolved carbon concentration since it: 1) does not have a slope of 1 and 2) the BBC signature is lighter indicative a freshwater influence. Saluda/Whitewater Formations The Saluda Formation (Ordovician) is a massive dolomite overlain by partially dolomitized, marine limestones of the Whitewater Formation (Ordovician) and underlain by interbedded, marine limestones and shales of the Dillsboro Formation (Ordovician)(Brown and Lineback 1966). The Saluda and Whitewater Formations extend into southern Ohio and Kentucky. The Saluda Formation has also been recognized as a member of the Whitewater Formation based on its restricted extent (Gray 1972). The Saluda dolomite has been interpreted as a lagoonal deposit with dolomitization occurring from hypersaline solutions resulting from evaporation of seawater (Martin 1975, Hatfield 50 » q It¥iv|-"(°{P{f‘)‘0!0.‘-{.r" QD CID- -2 -. 51 11 “J N LL ‘137‘ 618 0 Figure 16. Seroe Domi Isotope Data, versus ENC after Fouke et al. 1996 51 5180 €51! .70.! .L.. 2‘!‘ 1:“thL'-’;"—"'}',;",' I" r“ ..s N. .H. U 1968). The depositional model is based on the presence of large corals, Tetradium and Favistella, which surrounded the dolomitized lens of the Saluda Formation off the Cincinnati arch, and acted as a barrier to seawater (Hatfield 1968). Further evidence in support of a hypersaline interpretation is the presence of the ostracodes, Leperditia and Leperditella, which prefer a hypersaline environment (Hatfield 1968). In the Madison, Indiana area, the Saluda formation varies from interbedded, partially dolomitized fossiliferous grainstones and dolomicrite near the base to a massive laminated dolomicrite comprising the upper portion of the Saluda formation. The overlying marine limestones of the Whitewater Formation are partially to completely dolomitized peloidal grainstones. Three outcrops (Highway 421, Hwy 7 and Hwy 56 outcrops; Madison, Indiana) were compared (see Sampling Locations section for locator map). The Highway 421 outcrop has the most complete and thickest section of the Saluda and Whitewater Formations. At this locality, there is approximately 16 feet of vertical section of the Saluda Formation and 20 feet of vertical section of the Whitewater Formation. The transition between the Saluda (dolomicrite) and the Whitewater (peloidal grainstone with abundant ostracods) is gradational over 8 feet of section. The upper portion of the Whitewater changes from a massive partially dolomitized limestone to interbedded shales and limestones. 52 ‘. 4- .n‘ .n. v- A. Q. . The Saluda consists of the upper massive dolomicrite, which contains minor laminations and the lower interbedded partially dolomitized grainstones and dolomicrite at the base. The predominant fossils in the partially dolomitized grainstones are brachiopods, bryozoans, crinoids and trilobites. The massive dolomicrite represents approximately 10 feet of vertical section and the lower interbedded section represents 6 feet of vertical section. In the lower section, the interbedded dolomicrite persists laterally. The grainstones occur as irregular, discontinuous lenses ranging from 4 to 22 feet laterally. Both the interbedded grainstones and dolomicrites thickness vary between 1 and 3 feet vertically. There are sharp boundaries between the interbedded grainstones, interbedded dolomicrites, and massive dolomicrite. At the Highway 7 and 56 outcrops, the total section is thinner. Cores of this section also indicate thinning eastward (Gray 1972, Brown and Lineback 1966). At the Highway 7 outcrop, formations above the Saluda have been eroded. There is approximately 10 feet of vertical section of the Saluda present. The interbedded grainstones and dolomicrites have the same lateral extent but do not exceed 1.5 feet vertically. The lower portion of the Saluda comprises only 4 vertical feet of section. At the Highway 56 outcrop, both the Saluda and Whitewater Formations are present. The Saluda at this outcrop is represented by 4 53 §.. ) vertical feet of section. Half of the Saluda section is represented by interbedded grainstones and dolomicrites. Individual beds range from a few inches to 2 feet thick. The transition between the Saluda and the Whitewater is gradational, similar to the 421 outcrop. Approximately 10 vertical feet of the Whitewater Formation (peloidal grainstone) overlies the Saluda Formation. At both the Highway 421 and 56 outcrops, the Whitewater Formation is overlain disconformably by Silurian limestones. Dolomite crystals in the Saluda Formation and overlying Whitewater Formation share the same zonal stratigraphy (Figure 17, 18). The same zone patterns indicate the two formations were dolomitized by the same solution (Sibley et al. 1993, Meyers 1974). Dolomitization of the Saluda and Whitewater Formations concurrently is in direct contrast to the idea the Saluda Formation was dolomitized penecontemporaneoulsy with deposition of the fine lime mud in a hypersaline environment (Martin 1975, Hatfield 1968). This does not indicate the Saluda precursor limestone was not deposited in a hypersaline environment but that dolomitization occurred after deposition of both the Saluda and Whitewater formations. The linear covariance between dUC and dwO values is consistent with dolomitization from a mixed meteoric—marine water rather than hypersaline solution (Figure 19, Table 3) (Lu and Meyers 1998, Frank et al. 1995). In this particular case, the total dissolved carbon 54 .AwaouoHE Ow M Qqu HO mmcoN pmuwucsooco HHm ocHuHQsto mHmumxuo Ou ucHOQ mzouu¢ .Hmumzuo wuHEoHop mdemm mo 36H> unmomwcHEdHopozumo .bH musmHm 55 .AmcouoHE OOH n SUCH HO mocoN CommDCSoocw HHm OCHDHQHwa Hmumxuo on mucHOQ zouufi .Hmummuo ouHEoHop kumzoanz Ho 3mH> DcoomocHEDHoponumo .mH muson 56 ]| 1 v 813C d» 818 0 Figure 19. Saluda and Whitewater Isotope Data SMO versus BBC 57 Table 3. Carbon and Oxygen Isotope Data Whitewater Formations 5 (VPDB) 0.78 1.05 .12 1.03 -0.09 0.29 .45 .84 .04 .88 .02 .65 1.27 1.27 58 for Saluda and concentrations of the two fluids would be the same. The dUC and dmO values also fall within the range expected for precipitation from late Ordovician seawater. However, this is inconclusive based on the large ranges in dUC and dmO (4 and 6 o/o.,ranges) obtained from brachiopods (Qing and Veizer 1994) and the general disagreement between workers on the best isotope values for Ordovician seawater. The massive dolomicrite is a unimodal planar dolomite with minor bioturbation and lamination and is interpreted as a massive mudstone (Figure 20). The Whitewater Formation is also comprised of a unimodal planar dolomite. In the Whitewater, ostracodes are only partially replaced and relict outlines of peloids are common (Figure 21). The Whitewater is interpreted as a peloidal grainstone. Dolomite rhombs nonmimetically replacing compacted ostracodes indicates dolomitization was postdepositional (Figure 22, 23, 24). The boundary between the Saluda and Whitewater is marked by a transition from laminar dolomicrites lacking fossil evidence to the partially dolomitized peloidal grainstones in the Whitewater Formation. In the lower section of the Saluda, grainstone lenses grade eastward from the Highway 421 outcrop into packstones (Figure 25, 26) and wackestones (Figure 27, 28, 29, 30) interbedded with dolomitized mudstones at the Highway 56 and 7 outcrops. 59 Ho Eouuop paw Qou ou ucHom mzouufi .AmcouoHE OON u SUCH Hv GoHumcHEMH .wcoumpse mdemm Ho 3oH> uanH CHMHm .om musaflm 60 mucHom 30HM< .chouoHE OOH n aqu HO pHonQ mo mcHHudo uoHHmu ou .mcouqumum HmpHonQ kumeanz mo Sme mumHom powwouo >HHmHuumm .HN mudem 61 is.— ampmoflaqflv .AmcouoHE OOH u noaH HV mmpoomuuwo owuowmaoo OcHomHQmu mH “sounm >b naoau muflsoHoa .ocouqumum HmpHonQ umumzwans Ho sz> unoHH chHm ..¥.v r .\« .NN mnaon 62 63 50 microns). (1 inch Closeup View of dolomite rhomb in Figure 22 Figure 23. .AmcouoHE OON u socH HV mooomuumo cm ocHodewu bfionu wuHEoHoo ou mucHoa 30nn< .mcoumchuO HmpHonQ umumzwanz Ho 36H> uanH chHm .vm musmHh HHmmOG ou wchOQ sound .chouoHE OON n nocH HO ucwammuu .wcoumxoma mosHmm HQ sz> mHMHOQ pmwmouo >HHmHuumm .mm wuson 65 T, t t: .. F. >. HHmmou ou mucHoa 30nu< .AmcouoHE OON n nocH HO uquomuw .mcoumxomm mpsHmm Ho 36H> mumHoo Ummmouo >HHmHuumm .GN musoflm 66 oHocHuo ou ucHom mZOHHd .AmcouoHE OON u nocH HO mudwfiOmuw .mcoummxomz mdemm Ho 36H> wumHoa pommouo >HHmHuHmm .sm mHDOHm 67 pHocHuo ou mucHoa zouum .AmcouoHE OON n aoGH HO unmammnm .wcouwmxomz mpsHmm Ho zme mHmHom pmmmono >HHmHuumm .mm musmHm 68 pHooHuo ou mchoa zouu< .AmcouoHE OON u nocH HO ucmEOmuH .mcoummxomz mdemm Ho 36H> mumHoo ommmouo >HHmHuumm .mm wusmnm 69 -— «W v‘ s ”f. . cmoNo>uQ ou mucHoa zouu< .chouoHE OON u nocH HO ucmfiomum .mcoumwxomz wpsHmm MO on> mumHom powwouo >HHmHuHmm .om musmflm 70 Mbthods Dolomites representing different lithologies, ages and stable isotope signatures were chosen to compare zone-width (growth rate) vs. crystal-size relationships (Figure 31). The consistent zonal stratigraphy between the Whitewater Formation and Saluda Formation allowed comparison of mudstones, grainstones, packstones and wackestones. Wackestones from the Burlington-Keokuk and Saluda, which have distinctly different dolomitizing fluids, (based on stable isotope signatures) were used for comparisons between similar precursor lithologies of different ages (Figure 8, 27-30). The Seroe Domi exhibited more than one concentric zone free of zonal unconformities (episodes of alteration or dissolution between precipitation of individual zones) bounded by at least one internal and external zone. This allowed comparison of zone width-crystal size relationships through time. Zone Selection A zone must represent the entire period of precipitation, or be free of zonal unconformities, and be preceded and succeeded by a zone to accurately reflect growth rate. If the central zone is chosen, differences in time for primary nucleation could account for differences in zone width since the type of substrate has been shown to affect the length of the induction period, or time to first 71 6 13 C ‘4‘. A A A A. 1.1’ A “‘ ‘A 2 — ‘ ‘ of ‘ ‘ A108 °. AA . wt I fiv- 1 -6 -4 ‘2 2 4 -2_ I -4- a. I II -6-- I l' 8 5 18 O [oSaluda.ISeroe Domi ABurlington—Keokuk Figure 31. 72 Isotope Data, 8180 versus 513C heterogeneous nucleation (Sibley et al. 1994). This effect is minimized during secondary nucleation of dolomite on dolomite. The outermost zone is commonly found to exhibit dissolution or intergrowth preventing an accurate measurement of zone width. In addition to these restrictions, only concentrically zoned, rhombic slices of the crystals in thin section are measured in order to convert apparent zone width to true zone width (see Geometric Corrections Section). Sampling locations Samples of the Saluda, Whitewater, and Burlington- Keokuk Formations were collected from four outcrops. Thin sections for the Seroe Domi Formation were provided by Bruce Fouke (see Fouke et al. 1996). The Saluda and Whitewater formations are represented by three outcrops along an east to west trend near Madison, Indiana (Figure 32). The Burlington—Keokuk Formation crops out along Highway 61 north of Bowling Green, Missouri (Figure 32). Samples were collected on a grid from the four outcrops (Figure 33, 34, 35 and 36). The Seroe Domi formation thin sections are from transits along two adjacent outcrops (Figure 37, after Fouke et al. 1996 and Fouke, unpublished field notes). Sample locations are indicated on the profiles of the three outcrops of the Whitewater and Saluda dolomite at the Highway 421, Hwy 7 and Hwy 56 outcrops in Southern Indiana 73 0 80 160mi \ —::l m Outcrops Illinois Indiana Missouri I Burlington Keokuk Outcrop Madison E." Indiana 7 .421 Figure 32. Location Map 74 ou muqum zoumfl .mpsHmm Ho mmmn um um>mH Hmuoo .wcoHumEuom umpmSwuHaz paw mosHmm Ho monoudo Hmv >m3cmHm .mm wHSOHm 75 Hmuoo ou muqua Zonufi .mpsHmm Ho wmmn um uwmmH .mcoHumauom uwumzmanB pom mosHmm Ho dououso n >mBnOHm .vm mHDOHm 76 Figure 35. Highway 56 Outcrop of Saluda and Whitewater Formations. Arrow points to coral layer at base of Saluda. 77 .coHumSuom xsxooxlcouocHHusm Ho gououso HO >mznOHm .mm wusmHm 78 Amouoc oHoHH pmsmHHQSQGS oxsom paw mmmH .Hm no 330m “5pr omomuso .mmououso musanmHnon 2.6 pam cmpcmHm swam .HEoo moumm .bm wusaflm \\\\ . \s.\\\\ \ \\\ \\\x\\\\> \ .. . . xxx. _. \k« \ \\ \.\\\ z m OanmHmHnon .um cmpqum snow Ommnlo .3 .ON .o 79 (Figure 38, 39 and 40). The three outcrops occur across a transect approximately 5.5 miles in length (Figure 32). At the largest outcrop, the Highway 421 outcrop, samples were collected along 435 feet of exposure. Samples were collected in grids at a spacing of 3-5 feet vertically and horizontally where possible as indicated on the outcrop profiles (Figure 38, 39 and 40). A similar grid sampling was employed for collection at the Hwy 61 outcrop of the Burlington-Keokuk in Eastern Missouri covering a distance laterally of 363 feet (Figure 41). Samples from the Seroe Domi represent three small dolomitic lenses less than 15 feet long and 3 feet thick (shaded beds in Figure 37). Only three widely spaced samples were analyzed due to significant replacement and dissolution of generation I dolomite in the Seroe Domi Formation. ZOne.Mbasurements .A Luminoscope Model ELM 3.3 operating at 16kV was used to observe the cathodoluminescence of dolomite in polished thin sections of the four formations. Color slide pictures were taken from thin sections of the samples. The slides were then examined with a light microscope for rhombic slices of dolomite. Rhombic slices of dolomite that exhibited concentric zoning and parallel zone apexes were measured (Figure 42). The length measurements A, B, C and E are used to correct slices that cut the center of the 80 2d «82.83 8. ”an E. a. “no a. mans“ mg.- mg. a a a a a s as... 82 82-82 mHHuoum nonouso Hme >32 mvsHmm .mm ouson o.oo-IoQAWNIZOmquo-ooooI—oOOQMIQmINK‘I‘mW-IWJ—Iamo on. Gdamnlcvsmb nofloonooAAAOooo Elm—m ......°m_.l.s..m.. Hakka..." as. 38 .. ... am 2235 AnaaabdggeGanneaxse 8868—83 3 88653» was 8:382: mung—a . . Aassaeaeosaaau o. .amsanm _HHHHuIIII- .o GEO—on .m 368 H ~ .0m .3 .o 2“ . aasaa\\ u N no as 328 8283! .H. A .2 u L Hoaom 86> . . .k 1. . .I. a 8.8m _Sconcom @228 ago . , Om H . .. 885....» 3222. d. .. 5.322.: ms m .m> .2 81 oHHHoum dououso h >3m mosHmm .mm wHSOHm ”I .v .N .O o o O I o o o o o o o If as: was .15 a... if 1..— Z... «.5 2.5 :1”... . N O I I I I I O I 0 V «£8. n68. neck v.8... finch «-89 968. 2.8% H 78,—. . o o I o o I 730: «.303 9303 v.30: 930$ 9303 ”Sam 82 n H I . , (l (1 . a: 932.5 H 1 (. V I IIII‘ , .. AN.\\\ \, .4” III . . . x . x. a . \ l . r 1 If [Will |llfli . , 6 \\ \ .l ‘— oaOumoxoSS 7 | : .v o , I J. \ \ s o II. Ill 5 1% . Em ans—um i. .N J )J 0:332: W * I! W \ (III! P l x N ‘V K m 025 5.52 >9 h meHHoum dououso mm 55 mpsHmm .Ov magma and 79». mud moan 530m 023 530m and two 3 3. Va 1. comm £82 .5“ 08i=5 Em EA... 00am 5.52 . 83 mHHHoum dououso Hm >25 MsxowxlcoumcHHusm .Hv mHDOHm 6% Oman . 2.1.5 2.3 . 2.6 a 3 . . .533 Sea 3.x: :..3 31 .13 2.qu $.qu 3..qu 3.03 24o 9.655 3.05.5 3.05.5 0905.5 . _Hl .mN .o 2.250 mum> 84 Lab". #9 v.3. Figure 42. Zone measurements of rhombic slice (shaded band represents zone measured) 85 crystal but not parallel to the l O l 4 face. Typically, zero to five crystals were found on each slide that cut through the center of the crystal at an angle to the 1 O l 4 face that could be corrected back to the 1 O l 4 reference plane (see Geometric Corrections section). Since all four formations lack an orientation of their crystals, each crystal has an equal probability of being cut in an orientation that allows measurement. Comparison for precision in length measurements between two independent observers indicates a correlation of 99% (Figure 43). The difference in measurements between the two observers is normally distributed indicating the error is not skewed towards smaller or larger crystals. Replicate analyses for the first independent observer have a 99% correlation (Figure 44). Replicate analyses for the second independent observer have a 98.5% correlation (Figure 45). The precision error on any single length measurement is +/- 1 tic unit. The precision error on the corrected zone width and crystal radius values is also +/- l tic unit. Geometric corrections Three categories of slice orientations can be used to calculate back to the 1 0 1 4 reference plane. Each of the three types of slices must cut through the center of the crystal. In order to insure this condition, samples from 86 ‘5 60 (D a 3 50 g _ U) a) g 40— £3; 4.) 3830— H m o H-H N520- 0 Z H 10‘ 0) :> g 0 ‘T V T l g o 10 20 30 4o 50 Observer No.1 length measurement (microns) Figure 43. Comparison of length measurements between two observers 87 25 20J 15~ 10. Replicate Set of Measurements Figure 44. 5 10 15 20 25 First Set of Measurements Comparison of replicate analyses for first observer 88 q 20 316 a 214- 8 5 12- 8 w 10« E u 8— o 23 6‘ U) m 4- 0.98 ‘5 o 2‘ 5' Q 0 , , , SE 0 5 10 15 First Set of Measurements Figure 45. Comparison of replicate analyses for second observer 89 each formation were inspected for slices that included the greatest number of zones. Only slices that exhibited these zones were measured. Slices of crystals that did include all the zones and thus cut through the center could be divided into three general orientations: 1) rotation through the long diameter of a rhomb, 2) rotation through the short diameter of a rhomb, and 3) rotation through both the long and short diameter. From measurement of the apparent zone width (C-E, Figure 42), apparent crystal diameter (E, Figure 42) and zone boundaries (A and B, Figure 42), true zone width and crystal radius can be calculated. (See Appendix A for a detailed description of true zone width and radius calculations). Statistical Methods A minimum of 30 crystals from each sample with paired zone width and radius data were plotted. Normal probability plots were used to determine radius and zone width distributions. The Shapiro-Wilkes normality test was used to test for a normal distribution. Regression analysis included linear, quadratic, and exponential fits. Rearrangement of the complex quadratic mononuclear growth model equation to a linear function was used to distinguish this case (see previous Population Trend Section for equation). To determine the goodness of fit of a sample to a regression line, the correlation coefficient was 90 determined. To determine if the relationship between zone width and radius of crystals from a sample was statistically significant, an f test of the correlation coefficient was used with the null hypothesis of no correlation between zone width and radius, or no slope (Crow et al. 1960). To distinguish between different slopes generated from different samples, a t test of regression coefficients was used to compare variances of the radius populations between the two samples and the variances of zone width populations between the two samples (Crow et al. 1960). This t test is referred to as the significance of B t test and is used to determine if the slopes varied between samples at the 95 percent confidence interval (Crow et al. 1960). In the B t test, the null hypothesis was no variation between the two slopes, or a difference of slopes equal to zero. Results Paired zone—width vs. crystal-radius data from the Saluda, Whitewater, Burlington-Keokuk, and Seroe Domi Formations can be described by both normal and log normal distributions. Crystal measurements for each sample are reported in measured tic increments, conversion to microns can be obtained by multiplying Saluda, Whitewater and Seroe Domi data by 1.5 and multiplying Burlington-Keokuk data by 1.0 (or unity) (see Appendix B for measurements). 91 Histograms of crystal sizes for each of the four formations indicate a near—normal coarse skew nature (Figure 46, 47, 48, 49). The characteristic coarse skew is often found in carbonate rocks as wells as other rock types (Eberl et al. 1998, Sibley et al. 1993). All of the samples can be characterized by a normal distribution at either the 95% or 99% confidence intervals, which permits the use of the significance of B t test and the f test of the correlation coefficient. The f test of the correlation coefficient is sensitive to the condition of normality. Deviations from normality result in lower coefficient correlations. Eighty—one percent of sample crystal sizes (r1) yielded normal distributions at the 95 percent confidence interval using the Shapiro-Wilkes normality test (Table 4). Eighty- five percent of sample zone widths yielded normal distributions at the 95 percent confidence interval (Table 5). Samples that did not meet the condition of normality at the 95 percent confidence interval, did meet the condition of normality at the 99 percent confidence interval (Table 6). Likewise, ninety-two percent of the sample crystal sizes yielded log normal distributions at the 95 percent confidence interval (Table 4, 5 and 6, samples denoted by *) and eighty-eight percent of sample zone widths yielded log normal distributions at the 95 percent confidence interval (Table 4, 5 and 6, samples denoted by +). All other samples can be described by a log normal distribution at the 92 450 400 q» ”'8 350 - 300 .- 250 4 200 + _, 150 + ~——' 100 ._ 50 4. o 1 frequency ] L I 4 l L l 7 r r I I T O 2 4 6 8 101214161820222426283032 crystal size Figure 46. Saluda/Whitewater Formation crystal size frequency 93 160 ‘— 1401 120-- 100«- 80-r frequency 40- 204 1 T 1 41 L ’n—h—h— T I r T 1 I " T T l 8 10 12 14 16 18 20 22 crystal size Figure 47. Burlington-Keokuk Formation crystal size frequency O ,5qu m u)- 94 25 ._———. 20~L 8‘ C 15«L (l) :3 3 H 10 .- q... 5 .L. O : .1 : : : ——l'—L_-J O 5 10 15 20 25 30 35 crystal size Figure 48. Seroe Domi Formation zone I crystal size frequency 95 7 4“; 3O 25 .L 20‘» Frequency H U1 10.- 5.» O r?— . 4+ + T—IT' 0 <1 2 4 6 8 10 bin Figure 49. Seroe Domi Formation zone II crystal size frequency 96 fl.— .10 ZHE *Hlmm mNQ ibmm .1QO .3 53 BE Lm $3 .5 13m th 40H m *m0 11me «m0 Lgov vmfi an m «mm «,Ofiwm .1va «.Hm E *m 30$ ‘69 ammm «omz «.AH mGONV Hmm *NN E «.H 30m «.mQ «.va ammz *AHH GGONV HEm am mfio .L” Wflm «.OHQ «.th *mz «.AH wCONV HEW .1th Adm umfi .4th *mm av: #AH wGONV Nmm *HH Mfim Lord «.MHQm *mHQm N2 «.AHH wGONv Hmm «mlwm .1va «.Hmm «.HHQm «.HZ Hm>umucfl oocoofiwcoo wmm man um maoflusnfiuumflo wuflm Hmum>uo Hmauoc spa: mmHQEmm .v magma 97 +Nez. +mmo +Hmma +mom +46 +Hm +mvm +so +NHQ ow mag +va +mo +mm +Hm mag oem em: +>Hm +m 30m +NN mm; +mmm +omz +AHH mucus «mm +H zom +m mac +vmm +mmz +AHH mcoNv Hzm +H yam +HH2 +st m2 +AH mcoNV HZm mam +omz +mm +vz AH mcouv Nmm +e>«_ +mmsz mfiam +mHm +AHH mucus Hmm «ma +mfimmo +HHQm +Hz am>umucfl mocwoflucoo wmm may um mcofiudnfluumao cube: ozoN amfiuoc cue: meQSMm .m magma 98 +05 mmq +AHH mcoNV Nmm +mmxmq +sm who +oH 2H2 +Nm who +1H mcoNv Hmm +o 2H2 +om mmq +mm UZDQ am who +85 2H: +ms< +smm +mm 2H2 +mmz +om ozpo +vmm +mHQm mH who +Nez +Nm who +UH< +Hmm H who He +vm who +on +emm +HH zoB +mo +mus gmm +mm +fimz +m wmm +eo +HH zoe +mo +mmz +vm< +NHQ +HH yam +mo +Ho +6H< +mmom +m wmwm +©Q +m0 *HHE *Nm +m-mm +mm +mmom +omz +>Hm Hnmm +oHo +Nz +Hmz +mHm moadfimm mmfldsmm mcoflusnfluumflo gnvfiz chN wgoaushfluumflo mNHm Hmumsno Hm>uwucfl oocmofiucoo wmm map um mcofluSQHuumflo Hmfinoc Spas mmaaamm .w magma 99 99 percent confidence interval (Table 4, 5 and 6, samples not marked). Zone width-radius scatter plots for 98% of all the samples indicate a statistically significant linear trend between zone width and crystal radius at the 95 percent confidence interval (Table 7). The slopes of individual samples from all four formations range from 0.05 to 1.53 with correlation coefficients ranging from 0.23 to 0.81 (Table 7). The mudstones, interbedded grainstones, packstones, wackestones and mudstones of the Saluda Formation each exhibit a linear correlation (Figure 50, 51, 52, 53, 54). Peloidal grainstones from the Whitewater Formation also exhibit a linear correlation (Figure 55). In addition, crinoidal wackestones from the Burlington-Keokuk and unimodal planar dolomites from the Seroe Domi exhibit a linear correlation (Figure 56, 57, 58). Plots of zone width-crystal radius (r1) for all samples from each of the three dolomites (Saluda/Whitewater, Burlington—Keokuk, Seroe Domi) are fit best by the equation dr/dt = kr. The data is not best fit by the crystal growth equations for populations of crystals growing by mononuclear growth, polynuclear growth, spiral growth, diffusion-limited growth or birth and spread growth. _ hug,"— Table 7. Slope and correlation coefficients for all samples Sample Slope r Sample Slope r M1Sm 0.15 0.62 HOW 1Sm 0.15 0.62 MZSm 0.22 0.76 HOW 6Sm 0.16 0.58 M4Sm 0.14 0.64 SAL 7-8Sm 0.14 0.41 M8Sm 0.10 0.45 PAY 11sw 0.21 0.74 M26Sm 0.11 0.52 56-1Sw 0.16 0.69 M30Sm 0.18 0.73 12.10”“ 0.16 0.43 M34“ 0.12 0.47 R5W° 0.21 0.45 6539 0.11 0.47 TON 11Sm 0.22 0.63 67Sq 0.15 0.65 PAY 5sw 0.16 0.61 3033'“ 0.11 0.66 A5dsm 0.11 0.44 SDllsm 0.19 0.69 Aldsm 0.21 0.62 31315Sm 0.13 0.44 56-5 W“ 0.11 0.27 95‘“ 0.08 0.45 A7g ”s" 0.12 0.35 p27wo 0.07 0.41 CAR 5*” 0.12 0.43 P36W° 0.16 0.65 LAK 223C 0.13 0.37 P40W° 0.14 0.45 LAK 31“ 0.16 0.37 P41“ 0.19 0.50 LAK 403° 0.16 0.46 1945“" 0.12 0.38 DFS 37“ 0.23 0.42 6659 0.14 0.69 LAK 103C 0.22 0.37 <38Sq 0.19 0.58 MIN 68C 0.23 0.60 065‘“ 0.26 0.81 DFS 243° 0.21 0.68 083‘“ 0.08 0.37 LAK 363C 0.41 0.76 010sm 0.12 0.43 MIN 168° 0.14 0.37 5073"“ 0.17 0.71 DFS 18‘: 0.18 0.44 181’“ 0.15 0.47 DFS 1536 0.11 0.41 P37W° 0.21 0.67 DFS 32 *“Bc 0.11 0.26 1319’“ 0.15 0.62 DUNC 56 “'80 0.05 0.23 P17W° 0.14 0.61 MIN 29 *“BC 0.10 0.28 P2... 0.06 0.41 SBl (zone 11)Du 0.62 0.59 s023s‘“ 0.10 0.49 5132 (zone I)Du 0.13 0.79 101 Table 7 (cont'd). Sample Slope r Sample Slope r G4Sg 0.11 0.47 SM1(zone I)**D” 0.05 0.24 01Sg 0.15 0.78 SM1(zone II)**D“ 0.87 0.34 M42Sm 0.07 0.39 8B2 (zone II)Du 1.53 0.78 M28Sm 0.11 0.59 5131 (zone IV)“ 0.19 0.43 M21Sm 0.19 0.63 Rf“ 0.17 0.47 1312Sm 0.11 0.64 025wo 0.14 0.56 M20Sm 0.13 0.37 034’“ 0.16 0.58 M11Sm 0.11 0.47 A7o1Sm 0.18 0.64 G339 0.23 0.61 A5gSp 0.17 0.64 P34 W“ 0.10 0.31 PAY 1sw 0.13 0.65 $013 *“S"‘ 0.10 0.27 * samples that have zero correlation at the 95 percent confidence interval # samples that have a significant correlation at the 89 percent confidence interval + samples that have a significant correlation at the 80 percent confidence interval COUUTJSU) "UZOBO Saluda Formation samples Whitewater Formation samples Burlington—Keokuk Formation samples Seroe Domi Formation samples dolomitized crinoidal wackestone unimodal planar dolomite where original rock texture is completely obliterated by dolomitization dolomitized peloidal grainstone dolomitized mudstone partially dolomitized grainstone dolomitized wackestone dolomitized packstone 102 zone width .0 5.0 Figure 50. 10.0 15.0 crystal size Saluda Mudstone 103 (sample M20) zone width Ol—‘wammxlm 104 .0 .0-- . .0—- , ° 0.. o - 0-- o. 0-- 0 : : : % . 0.0 5.0 10 0 15.0 20.0 25 30 crystal size Figure 51. Saluda Grainstone (sample G8) zone width .0 5.0 10.0 15.0 crystal size Figure 52. Saluda Packstone 105 (sample A5g) zone width 0.0 5.0 10.0 15.0 20.0 crystal size Figure 53. Saluda Wackestone 106 (sample Pay 5) NNUJU) zone width C)(J'IO(J'1OU'I(DU'1 O O ()1 O 10.0 15.0 20.0 25.0 crystal size Figure 54. Saluda Interbedded Mudstone (sample D12) 107 5.0+ . g4.0+ . "-1 3 3 0 ._ .. ... . 0 2 W 0. o o = 1.0-- o r 0.41 0.0 4 : f : 0.0 5.0 10.0 15.0 20.0 25.0 crystal size Figure 55. Whitewater Peloidal Grainstone 108 (sample P 27) zone width 0.0 5.0 10.0 15.0 20.0 crystal size Figure 56. Burlington—Keokuk Crinoidal Wackestone (sample DFS 24) 109 25.0 7.0-— 6.0-- 5.0-— 4.0-- 3.0<— 2.0-- 1.0«» 0.0 zone width 10.0 Figure 57. 15.0 20.0 25.0 30.0 crystal size Seroe Domi Dolomite, Zone I (sample SB1) 110 zone width O\ O «>- 4L T 0.0 2.0 4.0 6.0 8.0 10.0 crystal size Figure 58. Seroe Domi Dolomite, Zone II (sample 881) 111 . *.o’{,‘o-~(f19fi‘r’(i’h‘d\~:rt“€~l§£V"L‘ ' ‘ Comparison of Crystal Growth Rate Equation among Lithologies of the Same Dolomite In order to compare zone—width vs. crystal-size crystal growth equations among samples of the same lithology and samples of different lithologies, comparisons were made among samples of the Saluda and Whitewater formations since the same zone could be measured throughout the different lithologies of the two formations (dt is constant for samples compared). Because each sample is fit best with the equation dr/dt = kr, equations for different lithologies can be compared by slope. In the equation dr/dt = kr, k is the slope. However, unlike the other crystal growth equations for the crystal growth models previously discussed, the physical parameters that k signifies are unknown. In previous models, k is attributed to parameters such as solution chemistry and hydraulic properties. Because it is unclear what set of parameters k represents, k' will be used to denote the slope in the empirically determined crystal growth equation, dr/dt = k'r. Comparisons of k' among samples within a specific lithology and between samples of different lithologies indicated the slopes were not statistically different at the 95 percent confidence interval using the B significance test for slopes (Table 7). In addition, the mudstones and grainstones of the Saluda Formation and the grainstones of the Whitewater Formation sample slopes did not vary among or between 112 formations despite statistically different crystal size populations. Different rock types dolomitized concurrently did not exhibit a difference in the correlation between zone width and radius. Comparison of Crystal Growth Rate Equation between Different Dolomites The Saluda/Whitewater Formations, Burlington-Keokuk Formation and Seroe Domi all exhibit similar linear trends of crystal growth rate and crystal size. Each of the dolomites has a different zonal stratigraphy (dt is not assumed constant between different dolomites). Since the Burlington—Keokuk and Seroe Domi samples are also best fit by the equation dr/dt = k'r, comparison of crystal growth equations is accomplished by comparing the slopes. The slopes of the samples in the Burlington-Keokuk do not vary from the slopes of the Whitewater and Saluda Formations at the 95 percent confidence interval using the B significance test for slopes. The slopes of the Seroe Domi Zone I samples do not statistically vary from the slopes of the Whitewater, Saluda, and Burlington-Keokuk Formations at the 95 percent confidence interval using the B significance test for slopes. The slopes of the Seroe Domi Zone II samples do vary at the 95 percent confidence interval using the using the B significance test for slopes when compared to the Whitewater, Saluda, Burlington-Keokuk and Seroe Domi Zone I 113 samples. The mean zone widths for the Whitewater, Saluda, Burlington-Keokuk, Seroe Domi Zone I, and Seroe Domi Zone II do vary statistically from each at the 95 percent confidence interval using a two—sample t test comparing two formations at a time. Temporal Comparisons within the Seroe Domi Formation The unimodal planar crystals in the Seroe Domi Dolomite I exhibit two zones that can be measured. A dark zone and a light zone adjacent to each other in the crystals were measured (Figure 11). As previously stated, the slopes of Zone I and Zone II statistically vary from each other. The interior zone (Zone II) is a thick bright zone. The next zone precipitated is Zone I, a dark zone. Zone II is thicker than Zone I. Zone II is potentially composed of multiple thinner zones (Figure 11). These zones are individually not resolvable for measurement due to the difficulty in picking zone boundaries and the limit of magnification. Zone II samples have a greater slope than Zone I samples (Table 7). Comparison of Crystal Growth Equations for Adjacent Crystals in Thin Section Subsets of the Saluda and Burlington—Keokuk Formations were obtained by selecting crystals that share the same pore space or are in direct contact with each other (Figure 59). Plotting zone-width vs. crystal-size data for pairs of adjacent crystals results in a statistically significant 114 “swoonom ou ucfloa mzouum .Amzouofla 00H u goofl Hy mamum>uo Abouflmmv .oaasmw ouHEoHoo monamm Mo zoflb “GeomosflEDHooocumu .mm ousoflm 15 1 linear trend at the 95 percent confidence interval (Figure 60, 61). The Burlington-Keokuk subset was selected from data on samples LAK-22, MIN-16, and DFS—24. The Saluda subset was selected from data on samples M2, M1, M4, and SD3. Discussion The zone-width vs. crystal-radius plots indicate a similar linear trend, dr/dt = k’r, for all four formations. However, the linear crystal growth equation does not correspond to any of the published crystal growth mechanisms. The crystal growth equation dr/dt = k' r does extend spatially on the scale of an individual outcrop and on the scale of multiple outcrops separated by approximately five miles. Because the three different dolomites studied share the same general crystal growth equation, dr/ dt = k’r, the crystal growth mechanism can be said to be independent of lithology variation over the fluid composition range of dolomitizing fluids represented by the Saluda/Whitewater, Burlington—Keokuk and Seroe Domi dolomites. The extent to which k’ represents solution variation when comparing formations or different zones from the same formation is unknown since dt cannot be assumed to be the same between different zones or formations. The variation in the slope k' could result from solution variation, changes in dt, or some combination of the two 116 zone width 9 8 7 6 5 4 3 2 1 0 Figure 60. 10 15 crystal size Saluda Paired Crystals 117 zone width 10 15 20 crystal size Figure 61. Burlington-Keokuk Paired Crystals 118 25 factors unless the comparison of k’ is of values from the same dolomite and same zone such as the Saluda/Whitewater samples. Thus, the variation of k' between Seroe Domi zone II samples and all other samples may be attributed to both or either solution variation or a change in dt relative to the other samples. Crystal Growth Equation and Crystal Growth Mechanism The fact the relationship between zone width and crystal radius is linear and is not represented by any known crystal growth mechanism indicates either: 1) the linear relationship found represents a new mechanism or combination of mechanisms not investigated previously or 2) the assumption of isochronous zones commonly made in carbonate petrography is wrong. The assumption of isochronous zones can be made based on the assumption that changes in solution cause variations in zone intensity and color across the outcrop in a shorter period of time than the induction period for dolomite. Abrupt dolomite/limestone contacts and the lack of partially dolomitized rocks as well as experimental high temperature dolomitization of calcite indicate a long induction period for dolomite (Sibley et al. 1994, Sibley 1990, Sibley and Bartlett 1987, Sibley et al. 1987). Experimental studies also imply dolomite precipitating on dolomite seeds has a long induction period (Gaines 1980). This is consistent with the idea that changes in stochiometry of dolomite 119 -1- 3.. (percent molar Mg) affect the surface free energy requirement for precipitation. Thus, changes in stochiometry of dolomite with changes in solution could create induction periods between zones. Another argument that initial start times for zones are isochronous is the fact a random plot would be expected as a result of different-sized crystals starting at random times. While the previous argument indicates the initial time of each zone may be isochronous, the end time of each zone may still vary. If the final time for each zone is not the same, then a linear trend can be created by allowing the larger crystals a longer period of growth. However, if we look at actual data, this trend is found in each sample. So, if it is a matter of the larger crystals having grown for a longer time, then on the scale of a thin section, larger crystals grew for a longer time than other crystals in the area represented by a thin section. Pairs of adjacent crystals indicate the larger crystals either in the same pore or in direct contact with smaller crystals have thicker zone widths. Thus, the larger crystal is either 1) growing faster than the smaller crystal or 2) growing for a longer period of time. The latter would indicate the fluid around the large crystal was more saturated than the fluid around the small crystal and thus took a longer time to deplete even though the crystals share the same pore space. This of course, assumes the fluid between the adjacent 120 crystals was heterogeneous and not mixing, or solution in the pore was heterogeneous. This idea is rejected in favor of isochronous final times for zone widths. If large crystals were growing for a longer period of time due to solution heterogeneity, one would expect this trend to result from large crystals near pores. Petrographically, on the scale of a thin section there is no relationship between the large crystals and porosity (Figure 62). Large crystals and small crystals adjacent to each other that have no spatial bias to porosity and exhibit a linear trend between zone width and crystal radius, are readily found as indicated by the adjacent crystal pair plots (see Results Section). If the zones are isochronous as argued, the linear relationship found represents either a new surface-limited growth mechanism not previously considered, or a combination of crystal growth mechanisms that leads to a linear trend. Mononuclear, polynuclear and spiral growth mechanisms or any combination of these mechanisms will not result in a linear trend between zone width and radius among a population of crystals as the models are previously presented in the crystal growth literature. Diffusion-limited growth also does not result in a linear trend for a population of crystals. Birth and spread growth cannot be attributed to a linear trend among zone width and radius. Birth and spread growth assumes a constant nucleation rate/unit area and a 121 .Amconofla OOH u QUCH Hy xflupmfi cfinuaz cam whom umwc mamummuo momma ou ucfiom mzouu< .oaafimm xsxooxlcouocflansm uo Bmfl> mumaom powwouo >Hameuumm .No ousoflm 122 constant radial rate/unit area (Nyvlt 1985, Ohara and Reid 1973, Nielson 1964). In order to get a linear trend, nucleation rate or radial rate per unit area would have to vary from crystal to crystal. The saturation state would have to vary for adjacent crystals on a thin section for the nucleation or radial rate per unit area to vary for the previously published models. The latter variation in saturation state is rejected here for the same reasons it was rejected in the argument of isochronous final times for zone widths. There is no inherent property in any of the current growth mechanisms that would lead to a linear zone width—radius relationship in a population of crystals. An alternative, consistent with the data, is any combination of polynuclear or birth and spread growth with a modified spiral growth model or a modified spiral growth itself. The spiral growth mechanism varies only with saturation state or solution properties which effect precipitation (Christian 1975, Ohara and Reid 1973, Burton et al. 1951). The spiral growth model is independent of defect density to the extent that groups of defects or single defects on the surface independently contribute to the overall growth rate. In Burton et al. (1951), the rate of spiral growth is determined by the distance between steps of the spiral where the rate increases with the distance between steps: R = d (v00 /10) (Bennema 1984, Burton et al. 1951) 123 where X0 is the distance between each arm of the spiral, d is the thickness of the layer (step), and v w is the advance velocity of the steps (dependent on saturation state). The distance between steps produced by a spiral is given by the rate of step advance (v 00) per number of steps (determined by the distance between arms of the spiral) or the flux of steps, v m /10 (Bennema 1984, Burton et al. 1951). .A decrease in the distance between steps results in a solute uptake by the steps greater than solute delivery from solution. Thus, the crystal growth rate is dependent on the interrelationship between step distance and saturation state. As saturation state increases, the minimum distance between steps necessary to maintain a concentration of adsorbed ions around the step decreases. Burton et al. (1951) do indicate a range in growth rate is possible when more than one defect is present on the surface. In the case of a group of defects, Burton et al. (1951) divide the surface into groups of defects intergrowing and acting as one defect. In this case, the perimeter of each step is larger and overall growth is greater. However, growth is still limited by saturation state and the distance between steps resulting in the basic equation dr/dt = k. In either the case of single defects or groups of defects acting as one (due to intergrowth), if the distance between the defect centers or centers of defect 124 groups is great enough such that the center of the defects or defect groups do not intergrow then the total perimeter of steps is increasing. Simply, if the number of defects, whether single defects or group defects, on the surface is increasing, the rate of growth increases as the amount of step edge available or total step perimeter increases. Therefore, growth rate is dependent on defect density as well as distance between steps and saturation state. The crystal growth rate for a population of crystals interacting with the same solution would equal a constant, dr/dt = k, if the defect density/unit area/unit time did not vary from one crystal to another crystal. If the defect density/unit area/unit time increased with crystal size, then the crystal growth rate for a population of crystals interacting with the same solution could be represented by dr/dt = k*r where k* represents solution conditions, mineralogy, and defect density/unit area/unit time. Thus, crystals growing by the spiral growth mechanism in a homogeneous solution can still exhibit a linear population trend between zone width and crystal size where the larger crystals are growing faster by varying defect density. This could be accomplished in two ways: 1) an increase in defect density/unit area with crystal size or 2) increasing distance from defects originating in the center of the face to the edge of the face (an increase in defect density/unit area/unit time). 125 First, if the defect density/unit area varied with cryStal size, defect-ridden crystals would grow faster because the total step perimeter would be larger. Previously reported empirical evidence indicates larger crystals have a greater stress field to induce defects (Hull 1965). In addition, Randolph and Larson (1965) have indicated by observation some crystals inherently have more defects than others. Experimental evidence indicates a correlation between increasing defects and increasing growth rates (Ristic et al. 1991). Ristic et al. (1991) found an increase in the overall growth rate of potash alum crystals when incrementally increasing the strain on growing crystals. The increase in rate was attributed to an increase in dislocations observed petrographically on the growing crystals. Studies by White et al. (1974), Ottens et al. (1972), and Jancic and Garside (1975) also indicate an increase in crystal growth rate with crystal size but did not demonstrate a cause for the size—dependent growth. However, even if defect density/unit area was the same for all crystals, larger crystals could still grow faster if the defect density/unit area/unit time varied. A screw dislocation, the defect that causes spiral growth, is a slip plane in a crystal that occurs at an angle to the growing crystal face. The screw dislocation perpetuates in time by constantly supplying new low-energy sites for ions to attach to the surface relative to the formation of a 126 n:——.* __._V_ .. .z' c --... two-dimensional nucleus on a flat surface. As the defect perpetuates through time it grows at an angle to the growing face giving the appearance of migrating to the edge of the crystal surface. At the end of the life span of the screw dislocation it will intersect the edge of the growing crystal and the screw dislocation defect will become an edge defect that will not continue to propagate. To illustrate this point, the surface of a large crystal (crystal A, Figure 63) and a small crystal (crystal B, Figure 64) are divided into square unit areas and are given the same defect density/unit area. The lifespan of screw dislocations in the center of the larger crystal will be longer than the lifespan of screw dislocations in the center of smaller crystals. Thus, even if defects had an equal chance of occurrence/unit area (defect density/unit area is constant), larger crystals could still be growing faster than smaller crystals because the number of defects/unit area/unit time would be greater for the larger crystals. This is one alternative hypothesis for the physical model of the crystal growth mechanism represented by the equation dr/ dt =k'r determined from the empirical data in this study. Spatial and Temporal Crystal Growth Trends A crystal growth mechanism as described previously in the Population Trends for Crystal Growth Mechanisms section can be represented by a family of related functions since a crystal growth mechanism can occur over a range of solution 127 Figure 63. Crystal A 128 time time time time slice slice slice slice path of a defect originating in time slice 1 time slice 4 time slice 3 / / / / / / / / / F ] time slice 2 I 7 time slice 1 / / / / r/ /V/ 7 path of a defect originating in time slice 1 Figure 64. Crystal B 129 conditions. Also, when comparing formations, the period of time a zone grows can change the slope of the function but not the general function type. Thus, the four formations can all be described by the same general function type or crystal growth mechanism. The data indicate that bodies of rock on the scale of an outcrop that have the same net rock- water interaction and crystal growth mechanism, exist and are spatially mappable. Different lithologies within the Saluda/Whitewater Formations, different dolomites (Saluda/Whitewater, Burlington-Keokuk and Seroe Domi), and different zones from the same dolomite (Seroe Domi) have the same crystal growth mechanism, dr/dt=k’r. The slope of the fitted lines does not vary statistically from samples of one lithology to samples of another lithology. Thus, the crystal growth mechanism represented by the linear trend is not influenced by the range of the lithologies, rock ages or carbon and oxygen isotopes represented by the samples tested. Variance in Crystal Growth Equations (In the crystal growth equations, we find low to moderate correlation coefficients even though the trend itself is statistically significant. This variance from the fitted line may result from experimental error, solution variation across the thin section (distances much greater than the size of a pore) or variation in the amount of time 130 "' ‘2' .m’aarzms " a J— r" M the zone precipitates. First, the experimental error is discussed in the methods section and is less than the variation represented. Second, even though the pairs of adjacent small and large crystals in contact or within a pore indicate solution heterogeneity is not the cause of the linear trend, the variation from the trend may result from pore to pore solution heterogeneity. For example, if pore A solution has a higher saturation state than pore B solution, small and large crystals in pore A will grow faster than small and large crystals in pore B while the large crystals in both pores are growing proportionately faster than their smaller crystal counterparts. Arguments for the isochronity of initial and final times of zone widths are presented earlier. The constraint of a third unknown variable such as any solution concentration parameter (saturation state for example) for the zone measured and its relationship to the zone-width vs. crystal— radius function could result in a more accurate function with a corresponding higher correlation coefficient. In the Saluda/Whitewater dolomite, even though the slopes of the Whitewater samples and Saluda samples are the same, the mean zone width is greater for the Whitewater samples. This could be accomplished in two ways: 1) the saturation state was higher in the Whitewater samples and/or 2) the Whitewater samples were in contact with the dolomitizing solution for a longer period of time. In 131 either case, the trend of larger crystals growing faster than smaller crystals still occurs (Figure 65). Conclusions The Saluda/Whitewater, Burlington-Keokuk, and Seroe Domi Formations are growing by a similar mechanism as demonstrated by the same statistically significant linear trend, dr/dt = k’r, between zone width and crystal size for all four formations. The heterogeneity of the four formations compared agrees with previous work that indicates a single mechanism can operate over a range of solution conditions (Sunagawa 1984). The crystal growth equation does not statistically vary within a particular lithology or between lithologies when comparing the same zone. When comparing different formations, the same linear trend exists between two different zones. The crystal growth equation dr/dt = k’r also best represents zone-width vs. crystal-size plots of pairs of adjacent crystals. In addition, the data demonstrate the Saluda and Whitewater formations share the same zonal stratigraphy. From these observations, the following conclusions are drawn: 1) a body of rock greater than the scale of outcrop can be described by a single crystal growth equation, 2) the crystal growth mechanism represented by equation dr/dt = k'r operates over a range of conditions as represented by the variation in lithology, age, 132 zone width Figure 65. n o m c c o Tin-I m u m m o u H s o o u a c m-a -:-l U) 4U crystal radius Family of functions for dr/dt = k’r 133 carbon isotopes and oxygen isotopes of the Saluda, Whitewater, Burlington—Keokuk, and Seroe Domi Formations, 3) the higher growth rate of larger crystals is not a result of thin section-scale solute flux, and 4) the Saluda Formation was dolomitized after deposition of the Whitewater Formation in contrast to published work suggesting the Saluda was dolomitized in a hypersaline environment concurrently with deposition. While no current size-dependent crystal growth mechanism exists which can be ascribed to the equation dr/dt =k'r, this linear trend is found in similar data from Ristic et al. (1991), White et al. (1974) and Nordeng and Sibley (1996). A possibility suggested for the mechanism is a polynuclear, birth and spread and modified spiral growth or modified spiral growth with increasing defect density with time on the larger crystals. 134 ‘ . ..,.,.,,.“quanta-.1””(unfit-9:4. nit‘.":_‘tf_tfl('it§“FIR?"' APPENDIX A 135 APPENDIX A Geometric Correction to Slice of Rhombic Face Three lengths and one angle (A, B, C, B) were measured for each concentrically-zoned slice of the rhomb face (1 0 l 4) as illustrated in Figure 66. Measurement of B was used as an internal check on data precision since it can also be calculated from the three measured values of A, B, and C. The value of B calculated from A, B, and C in Equation 1 (Law of Cosines) was used to solve for the true lengths of A, B, and C referred to as A', B', and C'. B = cos”(Pf+B2—C2)/2AB] (Equation 1) Once B has been calculated, angles a and y can be calculated by applying the Law of Sines (Equation 2,3). 0 = sin”[(AsinB)/C] (Equation 2) y = sin*[(BsinB)/C] (Equation 3) Each of the three cases outlined in Figure 67 can now be solved. These three cases; Oblique Rotation (Case I), Rotation around the C—axis (Case II), and Rotation through the C-axis (Case III), are the only three cases which preserve a concentrically-zoned view with parallel apices. The three cases can be distinguished by the measured values as listed in Table 8. In Case III, C equals C' and no correction is required. For Case I and Case II, C' can be solved by comparison of the triangles created by; l) 136 A l4 c rl Figure 66. Slice Measurements 137 Case I — Oblique Rotation Case II — Rotation Around Long Diameter of Rhomb Face Long Diameter 3“ of Rhomb Face Case III - Rotation Around Short Diameter of Rhomb Face \ Short Diameter \ of Rhomb Face Figure 67. Three cases of rotation with corrections 138 Table 8. Parameters to distinguish Case I, II and III 139 bisecting C and 2) the normal to C’, which cuts through the apex, labeled with the angle B. In Case II, the line which is normal to length C' and the line which bisects C is the same line (Figure 68). In this case, length D' can be obtained by using the right triangle D'B(C/2). D' = B sin 0 (Equation 4) In Case I, the line that bisects C of the triangle ABC, is also the hypotenuse of the right triangle D'DX. The sides of D'DX are vectors (vector D' + vector X = vector D) which describe the orientation of the slice ABC relative to the triangle A'B'C' of the true rhomb face (Figure 69). The line that bisects C of the triangle ABC, or D, can be calculated from the Law of Cosines using triangle DB(C/2). D = [B2+(C/2)2-ZB(C/2)cosc5]1/2 (Equation 5) Once D is known, the angle 1 of the triangle DB(C/2) can be calculated from the Law of Sines. t = sin*[(Bsino)/D] (Equation 6) The angle A of the triangle D‘DX is a complementary angle to T. A = 180 - I (Equation 7) The length D' can be calculated from the right triangle D'DX. D' = D sin A (Equation 8) 140 C/2 Figure 68. Case II Solution 14] D' '31) X C/2 Figure 69. Case I Solution 142 For Cases I and II, B' and C'/2 can be calculated from the right triangle D'B'(C'/2) (Figure 70). In the triangle A'B'C', AF is equal to B' due to the symmetry of the rhomb face and o is equal to 7. From crystal symmetry, the angle B equals 73.2 degrees and 0 equals 53.4 degrees in the true rhomb face. Since the line D' equally bisects B, the angle 0 of the triangle D'B'(C'/2) equals 36.6 degrees. 8' = D'/(sin 53.40) (Equation 9) C' = (B'sin 73.2°)/sin 53.4‘D (Equation 10) Since E (Figure 66), the inner zone width, changes proportionately to C, E' can be calculated by scaling E by the amount C is shortened. E' = (C'E)/C (Equation 11) 143 C'/2 CI Figure 70. Triangle A’B'C’ 144 APPENDIX B 145 APPENDIX B Data Tables Table 9. Sample List for Saluda Formation Hwy 421 Outcrop Sample Sample Number Sample Sample Number Number ID of Number ID of Cr stals Cr stals ml 30 25 sd7 38 m2 33 26 sdll 31 m4 3O 27 sd13 36 m8 30 28 sd15 30 mll 31 29 sd23 30 m20 35 30 2 31 m21 30 31 5 30 m26 30 32 17 31 m28 33 33 19 30 m30 31 34 27 30 m34 30 35 31 3O 3O 36 34 30 33 37 36 39 31 38 37 37 43 39 40 34 32 4O 41 36 30 41 45 33 34 37 44 31 31 3O 36 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 146 Table 10. Sample M1 Measurements crystal zone .A B C E size width 25 28 32.5 27 12.9 2.6 14 19 21 17 7.4 1.7 29.5 32.5 38 32 15.3 2.9 42 41.5 51 42 20.2 4.3 45.5 39.5 56 45 19.0 4.6 23.5 25 29 25.5 12.7 1.7 24 22 28 23 11.1 2.4 26.5 25.5 33.5 29 12.8 2.0 24.5 24 29 27.5 13.7 0.7 35 35 43.5 33.5 15.7 4.7 17 17 17.5 16 8.0 0.8 21.5 20 27 23 10.0 1.7 40 39.5 47.5 39.5 19.7 4.0 12 11 13.5 11.5 5.8 1.0 11 11 12 10 5.0 1.0 43 45.5 57 49 21.6 3.5 18.5 18.5 25.5 23 9.0 1.0 18.5 20.5 20 16 8.0 4.4 30 40 38 33 16.5 4.6 28 25.5 32 29 14.4 1.5 45.5 49 57.5 50 24.2 3.6 26 28.5 33 28.5 13.9 2.2 45.5 48 58 50 23.5 3.8 22.5 21 26 21 10.4 2.5 25.5 21.5 29 26 12.2 1.4 25.5 28.5 32 29.5 14.8 1.3 46 48.5 58.5 51 24.0 3.5 19 22 22 18 9.0 3.7 30.5 35 38 33 16.5 3.2 16 14.5 18 16 8.0 1.0 147 Table 11. Sample M2 Measurements crystal zone A B C E size width 20 19.5 22.5 18.5 9.3 2.0 9 9.5 12.5 7.5 3.0 2.0 28 31 35.5 28.5 14.0 3.4 23 26 31.5 24.5 10 8 3.1 26 25 27 23 11.5 2.0 20.5 20 24 19.5 9.8 2.3 21 21 21 18 9.0 1.5 23 22 25 19 9.5 3.0 18 19.5 22 19 9.5 1.5 26 28 32.5 27.5 13.5 2.5 40 39 48 40 19.4 3.9 17 17.5 20.5 16.5 8.3 2.0 46 44.5 57 44.5 20.4 5.7 32 31 41 31.5 13.6 4.1 32 31 40 32 14.5 3.6 10.5 19 20 17 6.2 1.1 22 27.5 33 27 11.1 2.5 37.5 35 44 36.5 17 7 3.6 22 24 26 23 11 5 2.5 20.5 22 26 22 10.5 1.9 17 20.5 25 20.5 8.4 1.8 14.5 15 17 15 7.5 1.0 18 17 19 17 8.5 1.0 14 14.5 16.5 14.5 7.3 1.0 25 25 30 24.5 12 1 2.7 30 29 31 27 13 5 2.0 21.5 21.5 28 24 10.4 1.7 23 22.5 25 21 10.5 2.0 27 27 33 28.5 13.7 2.2 16 14 18.5 16.5 7.8 0.9 20.5 21 24 20.5 10.3 1.8 25 21.5 33 24 8.8 3.3 15 15.5 18 13 6.5 2.5 148 Table 12. Sample M4 Measurements crystal’zone A B C E size width 28 35 38.5 29 13.7 4.5 18.5 23 27.5 22.5 9.3 2.1 39 39 42.5 33 16.5 4.88 30.5 28 36.5 30 13.9 3.0 22.5 25 28.5 24 11.8 2.2 21.5 19.5 23.5 20.5 10.3 2.2 18.5 17 :22 18.5 8.7 1.6 42.5 42 48 38 19.0 5.0 34 32.5 34.5 27.5 13.8 3.5 17 20 23.5 17.5 7.8 2.7 23 23 26.5 22 11.0 2.3 22 23 25.5 20.5 10.3 2.5 26.5 21.5 30.5 25.5 11.4 2.2 20.5 21.5 24 19.5 9.8 2.3 16 13.5 19 15.5 6.8 1.5 14 13 16 14 7.0 1.0 9.5 10 10.5 6.5 3.3 2.0 15 12 16.5 12.5 5.9 1.9 21 17.5 23.5 18 8.6 2.6 36 34 43 36 17.2 ~ 3.3 18 19.5 19.5 17.5 8.8 1.0 24.5 24 28 24 12.0 2.0 24.5 31.5 35 26.5 12.0 3.9 29 26.5 38 29.5 11.6 3.4 15.5 15 16 13 6.5 *1.5 30.5 29 37.5 30.5 13.9 3.2 18.5 18.5 22 17 8.5 2.5 21.5 21 24 18.5 9.3 2.8 38 40 48 42 20.0 2.9 50 43 56.5 50.5 24.3 2.9 149 Table 13. Sample M8 Measurements crystal zone .A B C E size width 30 27 34.5 29 14.1 2.7 22 27 30 28.8 13.6 0.6 15 19 22 16.5 7.1 2.4 22 29 31 24 11.3 3.3 30. 26 35 28 13.1 3.3 18 18 22 18.5 8.9 1.7 19.5 16.5 22 19 9.1 1.4 17 22 24.5 20.5 9.2 1.8 16 18 20.5 16 7.8 2.2 34 32 41.5 36 16.5 2.5 15 15 19 16 7.3 1.4 20 20 24 20 9.9 2.0 19 22.5 26 22.5 10.3 1.6 12 10 13.5 10.5 5.0 1.4 23 22 26 21.5 10.8 2.3 32 25.5 37.5 30.5 13.0 3.0 19 18.5 22 20 10.0 1.0 26 32 35.5 29.5 13.9 2.8 17 15.5 22.5 18.5 7.1 1.5 22 20.5 23.5 19 9.5 2.3 25. 27 32.5 28.5 13.4 1.9 28 22 30.5 23.5 11.1 3.3 27 30 35.5 28 13.0 3.5 .29.5 35 43 33.5 13.8 3.9 21.5 21 26 20.5 9.8 2.6 _25.5 32 36 30 13.6 2.7 _1134.5 35.5 41 36 18.0 2.5 217.5 15 20 17 8.0 1.4 .__§1B.5 35 45 40 19.1 2.4 t___;34 34 41 35 17.2 2.9 150 Table 14. Sample M11 Measurements crystal zone A. B C E size width 19 17.5 22 19.5 9.6 1.2 26.5 24.5 29 23.5 11.8 3.8 26 24.5 27 24 12.0 1.5 13.5 14 16.5 13 6.4 1.7 19.5 23 28 23.5 9.9 1.9 20 22.5 27 23 10.3 1.8 24 21.5 28 23 10.9 2.4 24.5 25 28 25.5 12.8 1.3 29.5 27 34 29.5 14.5 2.2 20 15.5 22.5 19.5 8.7 1.3 27 29 31.5 30 15.0 2.2 13 15.5 18.5 15.5 6.7 1.3 16.5 17 17 16.5 8.3 0.3 26 29 34 29 13.6 2.4 16.5 14 19 16.5 7.6 1.2 19.5 18.5 22.5 21 10.5 0.8 18 20 22.5 20.5 10.3 1.1 20 18 23 22 10.7 0.5 17.5 19.5 21 19 9.5 1.8 14.5 14 19 16 6.6 1.2 25 26 26.5 22 11.0 2.3 13 12 14.5 11.5 5.8 1.5 24 27 32.5 27 12.1 2.5 17.5 15 19.5 16 7.9 1.7 15.5 14.5 17 15 7.5 1.0 26 27.5 32 26 12.9 3.0 28 23.5 31.5 28 13.3 1.7 23 23.5 25 23.5 11.8 0.8 24.5 28.5 32.5 27 12.8 2.6 44.5 45.5 53 47.5 23.8 2.8 29 23 31.5 29 13.9 1.2 151 Table 15. Sample M20 Measurements crystal zone A B C E size width 41 37.5 49 38.5 17.8 4.9 28 28.5 34 28.5 14.0 2.7 26.5 26 38.5 28 9.6 3.6 25 26.5 34.5 22 9.0 5.1 19.5 19.5 22 18 9.0 2.0 26.5 22.5 30 25 11.9 2.4 30 33.5 41 34 14.9 3.1 22.5 20 26 21 10.0 2.4 22 22 26 21 10.5 2.5 32 26 44 37.5 11.8 2.1 27 25 40 31.5 9.7 2.6 25 36 38 31.5 14.1 2.9 24 23 28.5 23.5 11.4 2.4 25 29 33.5 26 12.1 3.5 26.5 22.5 32.5 27 11.2 2.3 27 26 30.5 23 11.5 3.8 47 40 54.5 49 22.5 2.5 27.5 30.5 35 30 14.7 2.4 35.5 32.5 41 34 16.7 3.4 13.5 15 18.5 16.5 7.2 0.9 22 26 30 24.5 11.3 2.5 19 21 23.5 20.5 10.3 1.7 40 35 49 37 15.8 5.1 21 20 22 17.5 8.8 2.3 21 20 21.5 19 9.5 1.3 13.5 14.5 18 14.5 6.4 1.5 31 25 35 24.5 11.2 4.8 25.5 20 29.5 23.5 10.1 2.6 31.5 30.5 36.5 29 14.5 3.8 31.5 26 36 25.5 11.7 4.8 24 22 26 19.5 9.8 4.3 20.5 18.5 21.5 18 9.0 3.0 13.5 19.5 26 22.5 6.4 1.0 20 18 21 18 9.0 2.7 27 27 34 29 13.3 2.3 152 r 4 v Table 16. Sample M21 Measurements crystal zone A B C E size width 19 21.5 25 21 9.9 1.9 42.5 47 56 48 22.1 3.7 24 22.5 29 24 11.2 2.3 20.5 22.5 30 27 10.3 1.1 32 31 37 25 12.5 6.0 21 19.5 25 22 10.4 1.4 19 20 24 20 9.5 1.9 22 20 25 21 10.5 2.0 12.5 13 14 12 6.0 1.0 15.5 16.5 19.5 18 8.7 0.7 22 27 31 28 12.6 1.3 21 15 22 19.5 9.0 1.2 43.5 37.5 50 43.5 20.4 3.1 13.5 14 16 13 6.5 1.5 14.5 12 16.5 12 5.5 2.1 17 31 39 32 8.0 1.7 27.5 28 32.5 26 13.0 3.3 39.5 43 50 41 19.9 4.4 19.5 19.5 24.5 20 9.2 2.1 33 33.5 35.5 31 15.5 2.3 27 25 30 24.5 12.3 3.5 22 19.5 26 22 10.1 1.8 20 13.5 21 17.5 7.7 1.5 19.5 19 22 19 9.5 1.5 21 22.5 26 23 11.4 1.5 34.5 31 39.5 32.5 15.9 3.4 28 26.5 34 28.5 13.2 2.6 18.5 16.5 20.5 18 9.0 1.5 19 17 24 23 9.5 0.4 19.5 22.5 25.5 21 10.1 2.2 153 Table 17. Sample M26 Measurements crystal zone A B C E size width 14 15 19 14 6.0 2.1 18.5 14 20.5 19 8.5 0.7 13.5 12 16 14.5 6.7 0.7 29.5 29 29 25 12.5 2.0 22.5 22 26 22 11.0 2.0 22 17 26 23 9 4 1.2 12.5 19 20 18 7.7 0.9 21 20 26 23 10.4 1.4 20.5 26 29 23 10.5 2.7 30 33.5 38 33.5 16.6 2.2 20.5 26.5 29 23 10.7 2.8 15.5 15 18 15.5 7.8 1.3 22.5 18.5 25 22 10 5 1.4 27.5 28 34 30 14 4 1.9 21.5 18.5 25 23 10.6 0.9 19.5 16 22 19 8.8 1.4 8 8 10.5 8.5 3.6 0.9 32 33.5 44.5 37.5 15.0 2.8 10 15.5 16 14.5 6.3 0.6 28.5 28 33 28.5 14.3 2.3 19.5 24 27 24 11.1 1.4 16 18 19 17 8.5 1.9 17.5 19 23 19 8.7 1.8 18.5 20 22 19 9.5 1.5 28 28 35 30 13.9 2.3 32 26 35 32.5 15.7 1.2 16 14 17.5 15 7.5 1.5 29 30 35 31 15.5 2.0 15 15 18 16 7.9 1.0 24 22 25 22 11.0 3.3 154 Table 18. Sample M28 Measurements crystal zone A B C E size width 28 23.5 32 26.5 12.3 2.5 29.5 25.5 34 31 14.5 1.4 41 46 52.5 44 21.5 4.2 18 17.5 21 18.5 9.3 1.3 25 25 29.5 24 12.0 2.8 19 21 25 22 10.2 1.4 19 18.5 23.5 21 9.7 1.2 18.5 18 20 18.5 9.3 0.8 20.5 22.5 23.5 21 10.5 2.8 23.5 23.5 26.5 24.5 12.3 1.0 35.5 35.5 41.5 36 18.0 2.8 41 35 47 40.5 19.0 3.0 42 47.5 55.5 51 23.8 2.1 18.5 18.5 23 20.5 9.6 1.2 39 40.5 48.5 44.5 21.5 1.9 19.5 23 25.5 23.5 11.5 1.0 22.5 26.5 30.5 27 12.5 1.6 21.5 23.5 25 22.5 11.3 2.6 28 23 32 29 13.2 1.4 25 27 29.5 28 14.0 1.9 17 18 19 16.5 8.3 1.3 26.5 21.5 34 29 10.6 1.8 19.5 23.5 26.5 23.5 11.0 1.4 28.5 28 32 26 13.0 3.0 42 37 48 42 20.3 2.9 21 24 27 24.5 12.1 1.2 41 31 45 37.5 17.0 3.4 49 38.5 58 52 21.5 2.5 21.5 20 22.5 19 9.5 1.8 28.5 34.5 38 32.5 15.8 2.7 17 19 22 18.5 8.9 1.7 20.5 19 24 21.5 10.4 1.2 27.5 28.5 34 31 15.1 1.5 155 'Table 19. Sample M30 Measurements crystal zone A. B C E size width 27.5 25.5 34.0 27.0 12.0 3.1 31.0 21.0 37.0 32.0 11.3 1.8 31.0 31.5 36.5 27.5 13.8 4.5 36.0 38.0 44.0 37.0 18.5 3.6 39.5 42.0 51.0 42.0 19.4 4.2 37.0 37.5 43.0 35.5 17.8 3.8 32.0 27.0 37.0 30.0 13.7 3.2 39.0 36.0 49.0 39.5 17.0 4.1 23.0 29.0 33.0 27.5 12.2 2.4 37.0 37.5 45.0 39.5 19.4 2.7 36.0 39.0 47.0 39.5 18.2 3.5 14.0 12.0 17.5 15.0 6.1 1.0 37.5 32.0 44.0 36.5 16.4 3.4 23.0 23.5 27.0 22.5 11.3 2.3 15.0 18.0 20.0 16.0 7.7 1.9 19.5 18.0 22.0 20.5 10.3 0.8 20.5 21.0 25.0 22.0 10.8 1.5 42.0 39.0 48.5 43.5 21.6 2.5 36.5 34.5 41.0 35.0 17.5 4.0 25.0 23.5 32.0 29.0 12.3 1.3 12.5 14.0 15.5 13.5 6.8 1.0 18.0 18.0 21.0 19.0 9.5 1.0 15.0 14.5 18.0 16.5 8.0 0.7 27.0 28.0 35.5 31.5 13.8 1.8 16.0 16.5 19.5 17.5 8.7 1.0 19.0 16.0 22.0 20.0 9.1 0.9 24.0 26.0 28.5 25.0 12.5 2.7 28.0 28.5 35.5 33.0 15.2 1.1 16.0 16.0 16.5 13.5 6.8 1.5 50.0 42.0 56.5 50.0 23.6 3.1 14.0 19.0 21.0 18.5 8.1 1.1 156 "Z” in Table 20. Sample M34 Measurements crystal zone .A B C E size width 29.0 27.5 38.0 33.5 13.7 1.8 40.0 43.0 54.5 49.0 20.9 2.3 22.0 24.0 29.0 24.5 11.2 2.1 38.5 43.5 49.5 41.5 20.2 3.9 40.5 31.0 47.5 39.0 16.0 3.5 28.5 27.0 34.0 27.5 13.2 3.1 39.0 33.5 46.0 39.5 17.7 2.9 14.0 17.5 22.0 18.0 6.8 1.5 28.0 30.0 34.5 27.0 13.5 3.8 19.5 21.5 27.5 22.5 9.2 2.0 28.5 30.5 34.0 27.0 13.5 4.4 25.5 24.0 27.5 21.5 10.8 3.0 27.0 27.5 39.0 32.5 11.8 2.4 29.0 25.0 32.5 27.0 13.2 2.7 29.0 36.0 42.5 36.0 15.3 2.8 16.0 14.0 18.5 16.0 7.5 1.2 26.5 26.0 36.0 31.5 12.4 1.8 28.5 25.5 34.5 30.0 13.4 2.0 28.5 28.0 36.0 30.0 13.5 2.7 30.0 35.5 40.5 36.0 16.8 2.1 28.0 29.5 36.5 31.5 14.2 2.3 35.5 32.0 40.5 36.0 17.8 2.2 25.5 24.5 32.0 26.5 11.8 2.5 24.0 22.0 28.5 23.5 11.0 2.3 19.0 20.5 20.0 15.5 7.8 2.3 27.5 25.5 32.5 29.5 14.1 1.4 35.0 27.0 39.0 30.5 13.7 3.8 25.5 16.5 28.0 26.0 10.2 0.8 20.0 20.5 25.0 19.5 9.2 2.6 12.0 13.0 15.0 13.5 6.7 0.7 157 Table 21. Sample M42 Measurements crystal zone A B C E size width 17.0 13.5 19.0 17.5 8.0 26.0 25.0 28.0 24.0 12.0 19.0 18.5 21.0 20.0 10.0 46.0 40.0 53.0 46.0 21.7 O O \l 2.0 0.5 3.3 27.0 24.0 33.0 29.0 12.6 1.7 20.0 22.0 24.5 22.5 11.3 1.4 24.0 25.0 26.5 23.5 11.8 1.5 19.0 24.0 27.0 23.0 10.4 1.8 15.0 15.0 18.5 16.0 7.6 1.2 34.5 28.5 40.0 32.0 14.3 3.6 30.0 27.0 38.0 31.0 12.8 2.9 26.5 26.0 27.0 24.0 12.0 1.5 26.0 21.0 29.0 27.0 12.6 0.9 21.0 21.5 26.0 22.5 10.8 1.7 32.0 33.5 37.0 32.0 16.0 2.5 30.5 33.5 41.0 33.5 14.9 3.3 26.0 25.0 29.0 27.0 13.5 1.0 18.0 20.0 20.0 17.0 8.5 3.4 19.5 19.0 26.0 21.0 8.5 2.0 19.0 20.5 26.0 21.5 9.1 1.9 32.0 27.0 37.0 31.0 14.2 2.7 37.0 39.0 48.0 45.0 20.5 1.4 24.0 30.5 35.0 28.5 12.4 2.8 38.0 32.0 51.0 46.0 15.9 1.7 23.0 25.0 28.0 25.5 12.8 1.7 22.0 28.0 30.5 26.5 12.5 1.9 14.0 14.5 17.0 15.0 7.5 1.0 30.5 21.5 33.0 29.0 12.6 1.7 17.0 18.5 21.0 17.5 8.8 1.8 56.0 56.0 72.0 66.0 29.2 2.7 158 'Table 22. Sample G1 Measurements crystal zone A B C E size width 21.0 29.5 36.5 31.0 10.7 1.9 58.0 52.0 69.0 57.0 26.2 5.5 17.5 23.5 25.0 22.0 10.3 1.4 26.0 21.5 30.0 27.0 12.2 1.4 20.0 21.0 24.0 20.5 10 3 1.8 29.0 24.0 32.0 28.5 13.8 1.7 17.5 16.5 20.0 18.0 9.0 1.0 13.0 16.0 17.5 14.0 6.8 1.7 17.0 22.0 26.0 21.0 8.6 2.0 26.0 24.0 28.0 26.5 13.3 2.1 48.0 51.0 59.5 52.5 25.9 3.5 28.0 18.5 29.0 22.5 9.9 2.9 26.0 36.0 41.0 36.5 14.9 1.8 21.5 20.0 23.0 18.0 9.0 2.5 14.5 16.0 19.5 16.0 7.1 1.6 26.5 35.0 46.0 41.5 13.4 1.5 31.0 32.0 41.5 34.5 14.6 3.0 21.5 21.0 26.0 22.5 10.8 1.7 16.5 16.5 18.0 16.5 8.3 0.8 19.5 18.0 23.0 20.5 9.8 1.2 16.5 15.0 18.0 14.0 7.0 2.0 31.5 32.5 38.5 33.0 16.3 2.7 17.0 13.0 18.5 14.5 6.7 1.9 38.0 33.0 45.0 37.5 16.9 3.4 19.0 24.0 27.0 22.0 10.0 2.3 24.5 23.0 29.5 24.5 11.5 2.3 17.5 16.5 20.0 17.0 8.5 1.5 14.5 17.0 19.0 16.0 7.8 1.5 20.5 24.5 27.5 22.5 10.7 2.4 13.0 18.0 20.0 17.0 7.2 1.3 15.0 16.5 22.5 19.5 7.1 1.1 14.0 16.0 17.0 16.0 8.0 1.1 16.5 18.5 22.0 19.0 8.7 1.4 159 Table 23. Sample G3 Measurements crystal zone A. B C E size width 26.0 26.0 32.0 27.0 12.8 2.4 40.0 47.0 56.0 48.0 21.0 3.5 15.0 16.0 17.0 14.5 7.3 1.3 17.5 16.0 23.0 20.0 7.8 1.2 19.5 21.0 21.5 20.5 10.3 0.5 34.5 24.0 38.5 30.5 12.5 3.3 22.0 26.0 29.0 24.5 11.9 2.2 15.0 21.5 22.5 21.5 9.8 0.5 27.5 27.5 33.0 29.0 14.4 2.0 20.0 21.5 27.0 24.5 10.6 1.1 15.0 14.0 16.5 15.5 7.8 0.5 32.0 32.0 38.5 34.5 17.0 2.0 25.0 23.0 24.5 22.5 11.3 4.0 19.5 20.5 24.0 19.5 9.6 2.2 14.5 16.5 18.0 17.0 8.5 0.8 29.0 26.5 40.5 33.0 11.5 2.6 21.0 22.0 25.0 23.0 11.5 1.0 23.5 24.0 26.0 23.5 11.8 1.3 16.5 17.5 20.0 17.5 8.8 1.3 26.0 22.0 30.0 27.0 12.4 1.4 14.0 14.0 16.0 14.0 7.0 1.0 15.0 14.0 17.0 16.0 8.0 0.5 38.0 55.0 63.0 49.0 19.0 5.4 23.0 23.0 27.0 22.0 11.0 2.5 25.0 28.0 32.0 30.0 14.6 1.0 20.0 23.0 27.0 24.5 11.2 1.1 27.0 27.5 38.0 29.0 11.1 3.4 28.0 25.0 33.0 27.5 12.8 2.6 20.5 21.0 25.0 22.0 10.8 1.5 19.0 29.0 30.5 27.0 11.5 1.5 18.5 23.0 26.0 24.5 11.1 0.7 160 ‘ "-’ 19198520159" 'Table 24. Sample G4 Measurements crystal zone .A B C E size width 17.0 23.0 27.0 22.5 8.9 1.8 30.5 28.0 38.0 27.5 11.9 4.6 18.0 19.0 23.5 17.5 7.9 2.7 17.0 26.0 27.0 21.5 9.3 2.4 32.0 27.0 37.0 27.0 12.3 4.6 23.0 24.0 28.0 24.0 12.0 2.0 34.5 37.0 46.0 35.5 15.7 4.6 29.0 25.0 32.5 24.0 11.7 4.2 29.5 28.5 35.5 26.0 12.5 4.6 28.0 23.0 33.0 26.5 11.5 2.8 13.0 17.5 19.0 14.0 6.3 2.3 17.5 23.0 26.0 19.5 8.5 2.8 19.0 26.5 29.0 24.5 10.6 2.0 18.0 21.5 25.0 20.0 9.0 2.2 26.5 21.0 31.5 28.5 11.8 1.2 63.0 62.0 80.0 69.0 30.8 4.9 21.5 39.0 41.0 31.5 11.5 3.5 17.5 15.5 21.0 16.0 7.2 2.2 25.0 39.5 45.0 35.0 12.6 3.6 34.0 33.0 44.5 36.5 15.3 3.3 39.0 37.0 48.0 40.0 18.2 3.6 42.0 42.0 44.0 33.0 16.5 5.5 42.5 43.0 47.5 42.0 21.0 2.8 27.0 27.5 33.0 25.5 12.4 3.7 16.0 17.0 19.0 15.0 7.5 2.0 42.0 42.5 49.0 42.0 21.0 3.5 27.0 28.0 33.0 30.5 15.1 1.2 15.5 17.0 20.0 15.5 7.4 2.1 31.5 28.0 36.0 29.5 14.3 3.2 22.0 27.0 30.0 26.0 12.3 1.9 26.0 27.5 32.0 25.0 12.4 3.5 30.5 27.5 35.0 30.0 14.7 2.4 21.0 26.5 31.0 26.0 11.0 2.1 16.0 15.0 18.0 15.0 7.5 1.5 23.0 16.0 24.5 19.5 8.6 2.2 29.0 31.0 40.0 33.5 13.9 2.7 38.0 38.0 47.5 41.0 19.0 3.0 161 Table 24 (cont'd). crystal zone A B C E size width 26.0 22.5 29.5 23.5 11.3 2.9 24.0 22.0 22.5 20.5 10.3 4.6 29.5 32.0 37.0 30.5 15.0 3.2 20.0 17.5 23.5 20.5 9.4 1.4 25.5 26.0 31.0 25.0 12.3 3.0 29.5 27.5 35.5 29.0 13.5 3.0 162 'Table 25. Sample G5 Measurements crystal zone A B C E size width 22.5 23.0 27.0 23.5 11.8 1.8 18.5 20.5 26.5 22.0 8.8 1.8 24.9 28.0 32.5 26.0 12.0 3.0 25.0 28.5 33.5 28.0 12.9 2.5 20.0 18.5 24.0 21.0 9.8 1.4 12.0 16.5 18.0 15.5 6.8 1.1 21.5 19.0 24.5 23.5 11.4 0.5 37.0 37.0 43.0 39.0 19.5 2.0 14.0 15.0 15.0 11.5 5.8 1.8 12.5 11.5 15.0 13.0 6.0 0.9 20.0 20.5 23.0 20.0 10.0 1.5 13.0 11.0 15.0 13.0 6.0 0.9 13.5 15.0 17.5 16.0 7.6 0.7 8.5 8.5 10.0 8.0 4.0 1.0 31.5 32.5 32.0 27.0 13.5 2.5 20.5 21.0 26.0 22.0 10.2 1.8 25.5 27.0 32.0 28.5 13.7 1.7 23.0 24.5 30.0 26.5 12.1 1.6 20.5 22.0 24.0 17.0 8.5 3.5 14.0 13.5 17.5 16.5 7.4 0.4 15.5 17.0 20.0 18.0 8.5 0.9 9.5 11.0 12.0 10.0 5.0 1.0 12.0 14.0 15.0 14.0 7.0 0.8 33.0 25.5 37.0 31.0 13.8 2.7 20.0 20A) 23.0 1915 9.8 1.8 33.5 26.0 36.0 31.0 14.8 2.4 15.5 16.5 20.0 17.5 8.1 1.2 23.0 23.0 28.0 26.5 12.8 0.7 21.5 21.0 28.0 25.0 10.6 1.3 26.0 21.0 29.0 25.5 11.9 1.6 21.0 22.5 25.0 20.5 10.3 2.3 22.0 28.0 30.5 27.0 12.8 1.7 163 Table 26. Sample G6 Measurements crystal zone A B C E size width 37.0 27.5 45.0 37.0 13.8 3.0 25.0 27.0 30.0 26.5 13.3 2.5 19.0 18.0 22.0 19.5 9.8 1.3 33.0 30.5 43.0 38.5 15.5 1.8 18.0 18.5 21.5 19.0 9.5 1.3 28.5 21.0 33.0 28.5 11.5 1.8 22.0 23.5 27.0 22.0 11.0 2.5 28.5 34.5 39.0 35.5 16.5 1.6 34.5 34.0 41.0 37.0 18.4 2.0 19.5 19.0 24.0 21.5 10.0 1.2 20.5 22.5 26.0 23.5 11.5 1.2 38.6 35.0 45.0 38.0 18.2 3.4 20.5 22.5 26.0 23.0 11.2 1.5 31.0 39.0 43.0 37.0 17.3 2.8 11.5 11.0 13.0 11.5 5.8 0.8 23.5 22.5 26.0 22.5 11.3 1.8 21.0 24.0 29.0 26.5 11.6 1.1 17.0 17.5 17.5 16.0 8.0 0.8 32.0 38.5 44.0 36.0 16.6 3.7 12.0 11.5 13.5 11.0 5.5 1.3 32.0 36.0 44.0 38.0 16.6 2.6 20.5 21.0 25.0 22.5 11.1 1.2 16.5 17.0 20.0 17.0 8.5 1.5 30.0 31.0 35.5 33.5 16.8 1.0 50.0 40.5 55.0 46.5 22.2 4.1 20.5 20.0 24.0 21.5 10.8 1.3 13.5 17.0 18.5 15.5 7.4 1.4 29.0 28.0 33.0 29.0 14.5 2.0 23.0 25.0 28.0 24.5 12.3 2.2 41.0 32.5 47.0 43.0 18.9 1.8 164 Table 27. Sample G7 Measurements crystal zone .A B C E size width 17.0 19.0 19.5 17.0 8.5 2.7 17.0 19.0 21.0 19.0 9.5 1.3 37.5 38.0 42.0 36.0 18.0 3.0 20.5 28.0 32.5 27.0 10.8 2.2 36.0 35.0 41.0 36.0 18.0 2.5 24.0 22.0 26.5 25.0 12.5 1.4 27.5 27.0 32.5 27.0 13.5 2.7 34.5 41.5 46.0 39.0 18.8 3.4 26.0 31.0 36.0 33.0 14.9 1.4 30.5 34.0 47.0 38.0 13.2 3.1 33.0 28.0 38.0 29.0 13.4 4.2 21.0 20.5 25.0 20.0 9.8 2.5 17.0 15.0 19.5 17.0 8.2 1.2 32.0 32.0 36.0 31.0 15.5 2.5 29.0 35.0 42.0 35.0 14. 3.0 14.5 10.5 17.0 15.0 5.8 0.8 20.0 22.0 25.0 23.0 11.5 1.0 33.5 37.5 43.0 38.0 18.5 2.4 19.5 21.0 23.0 20.0 10.0 1.5 36.0 37.0 44.0 37.0 18.2 3.4 37.0 36.0 44.5 35.0 16.9 4.6 20.0 26.0 30.0 26.0 11.0 1.7 15.0 13.0 15.5 13.5 6.8 1.8 21.0 24.0 27.0 22.0 10.8 2.5 18.0 26.0 28.0 23.0 9.9 2.2 40.0 40.0 48.0 42.0 20.8 3.0 14.0 13.0 15.0 14.0 7.0 0.5 22.0 23.0 27.0 23.0 11.4 2.0 17.0 17.0 24.0 21.0 7.8 1.1 42.0 40.0 52.0 46.0 20.8 2.7 22.0 17.5 24.0 22.0 10.5 1.0 27.0 27.5 30.0 27.0 13.5 1.5 25.0 26.0 29.0 24.0 12.0 2.5 18.0 17.0 20.0 18.0 9.0 1.0 165 Table 28. Sample G8 Measurements crystal zone .A B C E size width 22.0 24.0 27.0 23.0 11.5 2.3 36.0 35.0 39.5 32.0 16.0 3.8 18.0 18.5 18.0 17.0 8.5 0.5 28.0 26.0 35.0 29.0 12.6 2.6 34.0 32.0 40.0 31.0 15.1 4.4 30.0 31.5 36.0 32.0 16.0 2.0 31.0 32.0 37.0 32.0 16.0 2.5 31.0 31.5 37.0 31.0 15.5 3.0 37.0 41.0 47.0 34.0 16.7 6.4 31.0 31.0 37.0 31.0 15.5 3.0 48.0 54.0 62.0 54.0 26.1 3.9 30.0 32.0 40.0 35.0 15.4 2.2 31.0 32.5 40.0 35.0 16.0 2.3 31.0 29.0 36.0 31.0 15.3 2.5 23.0 25.0 27.0 23.5 11.8 2.9 16.0 18.0 20.0 17.0 8.5 1.7 20.0 18.0 22.0 20.0 10.0 1.5 45.0 40.0 52.0 42.0 20.1 4.8 22.0 20.0 26.0 21.0 9.9 2.3 27.0 27.0 28.0 23.0 11.5 2.5 36.0 46.0 52.0 44.0 19.5 3.6 34.0 35.5 37.0 32.0 16.0 2.5 15.0 16.5 18.0 15.0 7.5 1.5 30.0 34.0 40.0 34.0 15.7 2.8 36.0 30.0 42.0 37.0 16.5 2.2 44.0 43.0 50.0 44.0 22.0 3.0 36.0 31.5 44.0 37.0 15.9 3.0 42.5 43.0 51.0 43.0 21.5 4.0 20.0 26.5 29.0 26.0 11.8 1.4 22.0 20.0 22.0 20.0 10.0 3.2 24.0 24.0 27.0 25.0 12.5 1.0 17.0 14.0 22.0 18.0 6.6 1.5 16.0 18.0 20.5 18.0 8.8 1.2 32.0 29.0 37.0 25.0 12.1 5.8 19.5 20.0 22.0 19.0 9.5 1.5 32.C) 28.0 36.0 30.0 14.8 3.0 446.0 46.0 56.0 42.0 20.3 6.8 166 'Table 29. Sample D6 Measurements crystal zone .A B C E size width 38.0 35.0 47.0 41.0 18.1 2.6 31.0 37.5 44.5 35.5 15.3 3.9 33.5 28.0 39.0 32.0 14.3 3.1 28.0 19.5 30.5 24.5 10.4 2.6 34.0 37.0 68.5 57.5 5.8 1.1 26.5 31.0 34.5 27.5 13.5 3.4 31.0 32.0 34.5 28.0 14.0 3.3 31.0 33.0 38.0 29.0 14.5 4.6 12.0 13.0 15.0 12.5 6.2 1.2 19.5 15.0 21.5 18.5 8.4 1.4 11.5 11.0 14.5 11.0 4.8 1.5 27.0 26.0 31.5 26.0 13.0 2.8 27.0 30.5 35.0 28.0 13.5 3.4 49.0 40.0 54.0 45.5 21.8 4.1 33.5 28.5 43.5 38.0 14.2 2.1 29.0 20.0 32.5 29.0 11.7 1.4 22.0 16.0 24.5 20.5 8.8 1.7 44.0 35.5 51.5 43.0 18.5 3.7 13.5 13.5 16.0 12.5 6.3 1.8 21.0 19.0 24.0 20.0 9.9 2.0 16.0 20.0 22.0 18.5 8.7 1.7 20.5 27.0 30.0 25.0 11.1 2.2 18.0 16.0 21.0 18.0 8.5 1.4 22.5 21.0 26.5 22.5 10.9 1.9 23.5 24.0 25.0 19.0 9.5 3.0 20.5 20.5 24.5 20.5 10.2 2.0 42.0 27.0 44.0 36.0 15.2 3.4 24.0 19.5 27.5 23.0 10.3 2.0 31.0 32.5 38.0 30.5 15.2 3.7 17.5 18.0 21.0 16.5 8.3 2.3 24.0 23.0 28.5 23.0 11.2 2.7 18.0 18.0 21.0 18.0 9.0 1.5 42.5 35.5 50.0 38.5 16.9 5.1 23.5 22.5 25.5 23.0 11.5 1.3 35.0 30.0 39.0 31.0 15.2 3.9 32.55 29.0 41.0 33.0 13.7 3.3 4E3.0 43.5 57.5 44.0 19.5 6.0 167 Table 29 (cont'd). crystal zone .A B C E size width 47.0 50.5 59.0 44.5 21.7 7.1 20.5 22.0 25.0 21.0 10.5 2.0 22.5 20.0 28.0 21.5 9.1 2.7 27.0 32.0 37.0 30.0 13.7 3.2 20.5 22.0 25.5 21.0 10.4 2.2 18.0 19.0 23.0 18.5 8.6 2.1 30.5 30.0 33.0 29.5 14.8 1.8 168 Table 30. Sample D8 Measurements crystal zone .A B C E size width 39.0 37.0 47.0 40.0 18.9 3.3 31.5 35.0 41.0 36.5 17.2 2.1 26.0 27.5 29.0 26.0 13.0 1.5 29.0 31.0 35.0 30.5 15.3 2.8 29.5 27.5 35.0 30.5 14.5 2.1 33.0 33.0 40.0 36.0 17.5 1.9 26.0 36.0 40.0 36.0 15.3 1.7 29.5 27.0 34.0 30.5 15.0 1.7 32.5 32.0 40.0 35.5 16.7 2.1 25.0 23.0 28.5 24.0 12.0 2.3 26.5 24.5 32.0 29.0 13.3 1.4 15.0 17.0 19.0 16.0 8.0 1.5 18.0 23.5 27.0 23.5 10.0 1.5 21.0 21.5 26.5 22.0 10.2 2.1 25.0 24.5 32.0 28.0 12.3 1.8 18.0 19.0 21.0 19.0 9.5 1.0 23.0 19.5 26.0 23.5 11.2 1.2 29.5 35.5 40.0 36.0 16.9 1.9 35.0 34.5 42.0 37.5 18.4 2.2 23.0 18.0 26.5 22.0 9.5 1.9 24.5 25.5 29.0 25.5 12.8 1.8 38.5 35.0 48.5 38.0 16.0 4.4 28.5 27.0 31.0 25.0 12.5 3.0 14.0 13.5 14.5 11.5 5.8 1.5 24.5 23.5 31.5 27.5 11.7 1.7 27.0 28.0 35.0 28.0 12.6 3.1 19.5 22.0 25.0 20.0 9.8 2.4 17.0 16.5 20.5 17.5 8.4 1.4 21.0 34.0 34.5 28.0 12.0 2.8 21.0 27.0 30.0 24.0 10.9 2.7 25.0 21.5 33.0 26.0 9.5 2.6 169 a Table 31. Sample D10 Measurements crystal zone .A B C E size width 34.0 33.5 42.5 35.5 16.3 3.2 21.0 19.0 23.0 18.5 9.3 2.9 38.5 40.5 52.0 44.5 18.9 3.2 30.5 34.0 40.0 36.5 17.1 1.6 39.0 40.5 53.0 43.0 17.8 4.1 42.0 52.0 59.5 49.0 21.9 4.7 23.5 21.0 27.5 25.5 12.0 0.9 28.0 28.0 33.5 29.5 14.7 2.0 31.0 35.5 43.5 39.0 16.7 1.9 22.0 22.0 26.0 23.0 11.5 1.5 33.5 34.5 37.0 31.0 15.5 3.0 19.0 21.0 27.0 22.0 8.9 2.0 32.0 27.0 40.5 34.0 13.3 2.5 28.0 34.0 41.5 36.5 14.9 2.0 25.5 27.0 31.5 23.5 11.6 4.0 28.0 34.5 40.5 37.0 15.9 1.5 26.0 26.5 32.5 21.5 10.1 5.2 25.5 24.0 26.5 22.5 11.3 2.0 21.0 27.0 29.5 24.5 11.4 2.3 21.5 19.5 25.0 22.0 10.6 1.4 20.0 18.0 24.5 21.0 9.2 1.5 34.0 35.0 43.0 35.5 16.5 3.5 32.5 32.0 40.0 35.0 16.4 2.3 22.0 23.0 27.0 22.0 10.9 2.5 13.0 11.5 15.0 13.0 6.2 1.0 17.5 18.5 23.0 20.5 9.2 1.1 24.5 20.5 30.0 27.0 11.1 1.2 21.0 15.5 22.5 17.5 8.0 2.3 16.0 18.5 21.0 18.5 8.9 1.2 24.0 22.5 28.5 24.5 11.7 1.9 36.5 35.5 42.0 37.0 18.5 2.5 170 ‘J‘Z‘k" W w w ’33,; a; . tam: . p. .. . u 1 in ... up. .§..m.' . w it»... 1.. .. . .31 o 1: ;.. . .1. . 1.1!... 4... .. . a..x..¢.r$.€...¢.r1._...._.., __.... .. Table 32. Sample D12 Measurements crystal zone .A B C E size width 16.5 15.0 20.0 18.0 8.1 0.9 22.0 24.0 27.0 24.0 12.0 1.8 18.5 20.5 24.0 21.0 10.0 1.4 24.0 24.5 28.0 26.0 13.0 1.0 24.0 23.0 29.0 25.0 11.8 1.9 30.0 36.0 41.0 37.0 17.1 1.9 17.0 21.5 24.0 22.0 10.1 0.9 23.0 22.5 27.0 23.0 11.5 2.0 35.0 45.0 52.0 47.0 20.0 2.1 31.0 32.0 38.0 36.0 17.7 1.0 14.0 14.0 16.0 14.0 7.0 1.0 21.5 20.0 24.0 20.0 10.0 2.0 22.0 22.0 24.5 21.0 10.5 1.8 20.0 24.0 27.0 24.5 11.6 1.2 29.5 28.5 37.0 32.0 14.3 2.2 21.0 23.5 28.0 25.5 11.6 1.1 38.0 40.5 47.5 41.5 20.2 2.9 24.0 27.5 32.0 27.5 12.8 2.1 23.0 20.0 27.0 25.0 11.4 0.9 19.5 19.0 22.0 19.5 '9.8 1.3 39.0 38.5 47.0 41.5 20.2 2.7 20.5 20.0 24.5 22.0 10.8 1.2 39.0 37.5 47.0 42.0 20.0 2.4 30.5 24.0 38.0 33.0 12.4 1.9 19.0 20.5 26.0 23.5 10.0 1.1 24.5 24.0 28.0 25.0 12.5 1.5 20.0 21.5 24.0 21.0 10.5 1.5 13.5 13.5 17.5 16.0 7.0 0.7 28.0 29.5 35.0 28.5 13.8 3.1 28.5 27.0 36.0 30.5 13.3 2.4 171 winner . . A 9 7 1 . a A 5.... :..? . a .. o v .. ..... . :.. .vr :.. . _. ,-+...._........a... .4 . ._ .. . . 1 1 l . . _ l. .. . r .7...’ «J..Jsp.-._ . e . 1 .V . ”(Jew €.......;.......qwatwflaxflm.. .. ,1 Us... .1. ,. Table 33. Sample SD3 Measurements crystal zone .A B C E size width 29.5 27.0 37.0 32.0 13.7 2.1 35.0 36.0 43.0 36.5 17.8 3.2 46.0 57.0 66.5 56.0 24.3 4.5 36.0 37.0 41.5 35.5 17.8 3.0 57.0 45.0 63.0 55.0 25.5 3.7 40.0 35.5 50.0 42.5 17.8 3.1 38.5 38.5 50.0 42.5 18.5 3.3 16.0 19.5 22.0 17.0 7.9 2.3 34.0 35.0 38.5 33.5 16.8 2.5 24.5 23.5 29.5 24.0 11.4 2.6 38.5 52.5 57.0 46.5 20.8 4.7 21.0 22.5 26.5 22.5 10.9 1.9 18.0 19.0 22.0 17.5 8.8 2.3 17.0 17.5 19.5 14.0 7.0 2.8 21.0 20.0 23.0 19.5 9.8 1.8 14.0 15.5 17.5 13.0 6.5 2.3 12.5 12.5 15.0 12.0 5.9 1.5 19.0 19.0 23.0 18.0 8.8 2.4 36.0 33.5 42.5 35.5 17.0 3.4 25.5 25.0 29.5 25.0 12.5 2.3 28.5 27.5 31.0 26.0 13.0 2.5 24.5 25.0 27.5 22.5 11.3 2.5 26.5 20.0 31.0 28.0 11.4 1.2 24.0 22.0 27.5 22.5 11.2 2.5 31.0 30.0 35.5 31.5 15.8 2.0 19.5 18.0 23.0 16.5 7.9 3.1 36.0 39.0 46.5 41.0 19.2 2.6 52.5 42.5 64.0 53.0 21.3 4.4 35.5 36.5 41.0 35.0 17.5 3.0 28.0 22.5 33.5 24.0 9.9 3.9 35.5 35.0 41.5 36.0 18.0 2.8 19.0 14.5 21.0 17.0 7.7 1.8 43.0 45.0 53.0 42.5 20.9 5.2 26.0 25.5 28.0 21.5 10.8 3.3 12.5 14.0 15.5 12.0 6.0 1.8 31.0 30.0 32.0 24.5 12.3 3.8 172 ' -3xw.w , Table 34. Sample SD7 Measurements crystal zone .A B C E size width 35.5 32.0 46.0 31.0 12.3 6.0 35.5 30.5 41.0 34.5 16.0 3.0 17.5 17.0 18.0 14.5 7.3 1.8 14.5 14.5 17.0 14.5 7.3 1.3 20.0 24.0 29.5 26.0 10.6 1.4 27.5 37.0 41.0 35.0 15.4 2.6 39.5 39.5 47.0 39.5 19.8 3.8 50.0 44.0 57.0 47.5 23.0 4.6 14.5 14.0 15.0 13.0 6.5 1.0 19.0 17.5 19.5 18.0 9.0 0.8 19.0 19.0 22.0 19.5 9.8 1.3 18.0 17.0 21.0 17.5 8.7 1.7 17.0 18.0 20.0 18.0 9.0 1.0 29.0 29.0 29.0 26.5 13.3 1.3 35.0 27.5 39.0 33.5 15.3 2.5 49.0 44.0 59.0 50.0 22.5 4.1 34.0 36.0 40.0 35.5 17.8 3.6 34.0 28.0 37.5 33.5 16.2 1.9 33.5 32.5 42.0 36.0 16.2 2.7 48.0 44.0 58.0 48.0 21.9 4.6 28.0 30.0 35.0 30.0 14.7 2.4 41.0 31.0 45.5 39.5 17.5 2.7 27.5 30.0 35.0 31.0 15.0 1.9 42.0 31.0 46.0 39.0 17.3 3.1 43.0 33.0 49.0 43.0 18.5 2.6 14.0 16.0 17.0 15.0 7.5 1.6 11.5 12.0 13.0 11.0 5.5 1.0 13.5 13.0 15.5 12.0 6.0 1.8 17.5 20.0 23.0 19.0 9.0 1.9 18.0 18.0 21.0 17.5 8.8 1.8 27.0 30.5 35.0 29.0 14.0 2.9 26.0 29.5 36.0 28.0 12.14 3.5 18.0 18.0 21.0 18.5 9.3 1.3 18.0 18.5 21.5 17.0 8.5 2.3 30.0 35.0 42.0 36.0 15.7 2.6 18.5 24.0 26.0 21.0 9.9 2.3 23.0 14.5 23.5 19.0 8.2 1.9 173 fl *'-——r+ » wr'fi' "'2 “"+‘" Table 34 (cont'd). crystal zone 7 A. B C E size width I 30.0 I 33.5] 38.0 I 32.0J 15.8 I 3.0 ] 174 Table 35. Sample SD11 Measurements crystal zone .A B C E size width 33.0 20.0 35.0 28.0 11.0 2.7 29.0 29.0 34.0 29.0 14.5 2.5 34.0 49.0 53.0 43.5 18.7 4.1 32.0 32.0 47.0 33.0 11.3 4.8 32.0 32.0 34.5 25.0 12.5 4.8 35.5 41.0 53.0 46.5 17.9 2.5 48.0 37.0 51.5 43.5 20.7 3.8 14.5 13.0 17.0 13.5 6.3 1.6 15.5 16.0 18.0 15.5 7.8 1.3 19.0 21.0 23.5 18.5 9.3 2.7 17.0 16.5 20.0 18.0 9.0 1.0 28.5 27.0 31.5 26.0 13.0 2.8 26.5 24.0 31.0 25.0 11.9 2.9 17.5 10.0 18.5 15.5 5.8 1.1 27.5 20.0 30.0 25.5 11.3 2.0 26.5 23.0 31.0 26.0 11.9 2.3 16.5 11.5 18.0 16.0 6.8 0.9 18.5 26.5 29.0 25.0 10.6 1.7 24.0 26.0 33.5 28.5 11.7 2.1 29.5 28.0 33.5 28.0 14.0 2.8 40.5 33.0 47.0 39.0 17.2 3.5 14.5 14.0 15.5 13.0 6.5 1.3 29.5 29.5 35.0 27.5 13.8 3.8 13.0 13.0 15.5 12.5 6.3 1.5 32.0 31.0 40.5 34.5 15.3 2.7 17.5 16.0 19.5 17.0 8.5 1.3 18.0 20.0 23.5 18.5 8.7 2.4 21.5 21.0 23.0 19.0 9.5 2.0 24.0 25.5 29.0 22.5 11.3 3.3 17.5 16.0 20.5 16.5 7.9 1.9 12.5 11.0 14.5 11.5 5.4 1.4 175 Table 36. Sample SD13 Measurements crystal zone A B C E size width 18.0 18.0 20.5 19.0 9.5 0.8 36.0 35.0 44.0 38.0 17.9 2.8 27.5 27.5 33.0 31.0 15.3 1.0 25.0 28.0 33.0 29.0 13.5 1.9 27.0 25.0 35.0 26.5 10.8 3.5 19.5 21.0 24.0 20.0 10.0 2.0 20.0 21.5 26.0 20.0 9.2 2.8 25.0 23.0 31.0 26.0 11.4 2.2 18.0 19.0 21.0 20.0 10.0 0.5 26.0 23.0 31.5 27.0 11.9 2.0 31.0 35.0 40.0 35.5 17.2 2.2 26.0 28.0 34.0 29.0 13.3 2.3 17.0 16.0 19.0 16.0 8.0 1.5 23.0 24.0 27.0 21.0 10.5 3.0 27.5 21.0 30.0 25.0 11.5 2.3 19.5 18.0 22.0 20.0 10.0 1.0 23.5 28.0 31.0 26.5 12.9 2.2 20.0 18.5 23.0 20.5 10.2 1.2 22.5 20.0 27.5 23.0 10.0 2.0 27.0 25.0 31.0 25.0 12.5 3.0 18.0 16.0 17.0 16.5 8.3 2.6 21.0 21.0 25.5 21.5 10.4 1.9 13.0 20.0 21.0 17.0 7.2 1.7 20.5 15.5 22.0 20.0 9.4 0.9 25.0 25.0 28.0 22.0 11.0 3.0 16.0 14.5 20.0 15.0 6.4 2.1 21.5 19.5 24.5 20.0 9.9 2.2 25.0 26.5 28.0 22.0 11.0 3.0 20.5 21.0 23.5 20.0 10.0 1.8 29.0 22.5 33.0 29.5 12.9 1.5 29.0 29.5 36.0 26.0 12.4 4.8 22.0 23.0 27.5 22.0 10.6 2.6 29.5 30.0 38.0 30.5 13.6 3.4 32.0 30.0 34.0 28.0 14.0 5.2 19.5 19.0 21.5 16.5 8.3 2.5 18.0 17.5 22.0 17.5 8.2 2.1 176 o arc—+5 Table 37. Sample SD15 Measurements crystal zone .A B C E size width 33.0 32.0 41.0 34.5 15.8 3.0 18.0 19.0 22.0 19.0 9.5 1.5 19.0 20.0 24.0 18.5 8.8 2.6 22.0 19.0 25.0 16.5 7.9 4.1 21.0 20.0 25.0 21.5 10.4 1.7 16.5 15.0 22.5 15.5 5.6 2.5 20.0 20.5 23.5 17.0 8.5 3.3 42.5 49.0 64.0 52.5 19.8 4.3 29.0 28.0 32.5 26.5 13.3 3.0 22.5 25.0 30.5 24.0 10.6 2.9 19.5 23.0 25.5 19.5 9.6 2.9 35.5 35.0 39.0 30.0 15.0 4.5 19.5 22.0 26.5 18.5 8.2 3.6 32.5 34.0 36.5 27.5 13.8 4.5 36.5 37.0 50.5 39.0 15.3 4.5 24.0 24.0 31.0 24.0 10.5 3.1 19.5 24.0 26.5 19.5 9.3 3.3 19.5 25.0 31.0 23.5 8.8 2.8 20.0 24.5 27.0 20.0 9.6 3.4 35.0 29.0 41.0 31.5 13.9 4.2 26.0 26.5 32.0 27.0 13.0 2.4 24.0 24.0 30.5 23.5 10.6 3.2 27.5 28.5 29.5 24.5 12.3 2.5 31.0 32.0 30.5 25.5 12.8 2.5 13.0 11.0 18.0 13.5 4.4 1.5 23.5 28.0 36.0 29.0 10.9 2.6 20.5 18.5 23.5 18.5 9.1 2.5 41.0 31.0 44.0 37.0 17.3 3.3 25.5 23.5 32.0 29.0 12.5 1.3 21.0 17.0 23.0 21.0 10.1 1.0 177 Table 38. Sample SD23 Measurements crystal zone .A B C E size width 44.0 39.0 54.0 44.5 19.2 4.1 34.0 33.0 37.0 35.0 17.5 1.0 23.0 22.5 25.5 24.0 12.0 0.8 20.0 17.0 24.0 20.5 8.9 1.5 14.5 13.0 17.5 15.0 6.7 1.1 11.0 11.0 13.5 12.0 5.7 0.7 20.0 17.0 23.5 19.0 8.5 2.0 33.0 25.0 36.5 33.0 14.8 1.6 15.0 11.0 16.0 14.5 6.7 0.7 25.0 24.0 26.0 24.5 12.3 0.8 14.5 18.0 20.5 19.0 8.6 0.7 39.0 40.0 46.0 41.0 20.5 2.5 15.5 14.0 17.0 13.0 6.5 2.0 25.0 24.0 29.0 27.5 13.8 0.8 15.0 16.0 18.5 17.5 8.8 0.5 25.5 28.5 32.5 29.5 14.5 1.5 20.0 18.0 21.0 18.0 9.0 2.7 20.0 24.5 27.5 25.5 11.9 0.9 13.0 15.0 16.0 13.5 6.8 1.7 17.5 17.0 21.0 19.5 9.4 0.7 21.0 22.0 23.0 22.0 11.0 0.5 20.0 17.5 22.5 20.0 9.8 1.2 36.0 41.5 47.5 42.5 20.2 2.4 17.0 16.0 18.0 16.0 8.0 1.0 34.5 34.0 39.0 35.0 17.5 2.0 18.0 20.0 23.0 21.5 10.5 0.7 9.5 10.0 11.5 10.5 5.3 0.5 26.0 27.5 37.5 31.0 11.7 2.5 16.5 16.0 17.0 15.0 7.5 1.0 25.0 26.0 30.0 24.0 12.0 3.0 178 Table 39. Sample P2 Measurements crystal zone .A B C E size width 38.0 33.5 43.0 38.0 18.6 2.5 12.0 14.0 16.0 12.5 5.9 1.7 14.5 15.0 17.0 14.5 7.3 1.3 20.5 14.0 21.5 18.5 8.2 1.3 13.0 14.5 16.0 14.5 7.3 0.8 29.0 23.0 32.5 27.0 12.3 2.5 19.0 31.5 33.5 28.0 10.9 2.1 13.0 12.0 16.0 12.5 5.6 1.6 27.5 28.0 27.0 23.0 11.5 2.0 11.5 16.0 17.0 14.0 6.4 1.4 14.0 15.0 18.0 14.0 6.6 1.9 16.0 21.0 23.0 18.0 8.2 2.3 24.0 17.0 26.0 21.5 9.4 2.0 17.5 22.0 24.0 21.0 10.0 1.4 26.0 23.0 30.0 24.0 11.5 2.9 45.0 33.0 50.0 47.0 20.3 1.3 19.5 18.5 23.5 17.5 8.3 2.8 15.0 14.0 18.0 15.0 7.0 1.4 20.5 20.5 20.5 18.0 9.0 1.3 24.0 30.0 33.0 29.0 13.7 1.9 29.5 32.5 38.0 32.0 15.3 2.9 28.0 22.5 32.0 27.0 12.1 2.2 31.0 31.0 39.0 33.5 15.4 2.5 21.0 24.0 30.0 26.5 10.9 1.4 16.5 22.0 25.5 21.0 8.6 1.8 10.5 13.5 16.0 13.0 5.3 1.2 35.5 35.0 39.5 35.5 17.8 2.0 14.5 18.0 20.5 17.5 7.9 1.4 23.5 26.0 31.0 25.5 11.7 2.5 16.0 15.0 19.5 17.5 8.0 0.9 18.0 15.0 20.0 15.5 7.5 2.2 179 Table 40. Sample P5 Measurements crystal zone .A B C E size width 44.0 42.5 51.0 44.5 22.3 3.3 37.0 34.0 43.0 35.5 17.3 3.7 24.0 22.0 27.5 22.0 10.9 2.7 20.0 19.5 23.5 21.5 10.8 1.0 30.0 31.5 37.0 29.0 14.3 3.9 32.0 33.5 36.5 32.0 16.0 2.3 11.0 11.0 12.5 7.5 3.8 2.5 34.0 38.0 43.5 38.5 18.8 2.4 17.0 22.5 24.0 19.0 9.0 2.4 23.5 24.5 27.5 21.0 10.5 3.3 29.0 28.0 34.5 28.0 13.7 3.2 30.0 29.0 36.0 29.0 14.0 3.4 30.5 29.0 35.0 32.0 16.0 1.5 16.5 20.5 23.0 19.0 8.8 1.8 44.0 47.0 54.5 48.5 24.0 3.0 32.0 27.0 36.0 31.0 14.8 2.4 30.0 32.5 38.5 34.0 16.1 2.1 27.5 21.0 31.0 26.0 11.4 2.2 11.0 12.5 14.0 13.0 6.5 0.5 29.5 27.5 34.0 31.0 15.5 1.5 18.5 15.0 22.0 18.5 7.8 1.5 27.0 27.0 33.0 28.5 13.7 2.2 34.0 32.5 36.0 30.5 15.3 2.8 11.5 9.5 11.0 10.0 5.0 1.5 14.0 17.0 19.0 17.0 8.0 0.9 21.0 26.0 30.0 25.5 11.3 2.0 29.5 29.0 34.0 31.0 15.5 1.5 21.0 27.0 33.0 28.0 10.8 1.9 25.5 24.0 29.5 27.0 13.5 1.3 21.0 27.5 32.0 28.0 11.6 1.7 180 :..: 2.3:... . ......Qé......_. WNW... flawekuwx .2... tuna... I ...» . 3 _ .. _ .. :5. .... a.- ..Q .14.: ........,...-.....( .. _ .nijfa. ... $.14. fiufiedfifin .11 .... 5.. Table 41. Sample P17 Measurements crystal zone A. B C E size width 20.0 20.0 22.5 18.0 9.0 2.3 17.0 22.5 25.5 22.0 9.4 1.5 27.0 34.0 37.0 28.0 13.4 4.3 41.5 42.0 50.0 41.0 20.4 4.5 25.5 25.0 29.5 22.0 11.0 3.8 32.5 32.5 39.0 32.5 16.1 3.2 35.0 29.0 41.5 33.5 14.5 3.5 29.5 27.5 33.0 27.5 13.8 3.5 27.5 24.0 31.0 25.0 12.2 2.9 39.0 37.5 44.0 37.0 18.5 3.5 20.0 13.0 21.5 18.5 7.6 1.2 22.5 20.5 22.5 19.0 9.5 4.1 21.0 15.0 22.5 15.5 6.9 3.1 28.0 19.0 29.0 26.0 11.7 1.4 33.0 29.0 39.5 36.0 16.1 1.6 21.0 22.0 28.5 23.5 9.9 2.1 26.5 28.0 33.5 28.5 13.6 2.4 17.0 13.0 19.5 16.5 7.0 1.3 34.5 22.0 35.5 30.0 12.9 2.4 21.0 16.0 24.0 17.5 7.5 2.8 17.0 12.0 19.0 14.5 6.0 1.9 42.5 55.0 60.5 52.0 23.9 3.9 19.5 17.5 21.5 17.5 8.8 2.4 23.5 21.5 27.0 22.0 10.9 2.5 25.5 27.0 29.0 24.0 12.0 2.5 19.0 23.0 26.0 20.5 9.5 2.6 25.5 21.0 35.0 28.5 9.2 2.1 22.0 24.0 27.0 21.5 10.8 3.0 16.0 15.5 18.0 15.0 7.5 1.5 15.5 14.5 17.5 15.0 7.5 1.3 41.0 45.0 61.0 50.0 18.4 4.1 181 Table 42. Sample P19 Measurements crystal zone .A B C E size width 19.5 17.5 24.0 19.0 8.2 2.2 18.0 22.0 25.0 20.0 9.2 2.3 39.0 43.0 50.0 42.0 20.2 3.8 18.0 18.5 21.0 18.5 9.3 1.3 15.0 16.5 18.0 16.0 8.0 1.0 15.0 14.0 17.0 14.0 7.0 1.5 27.0 26.0 30.0 23.5 11.8 3.3 15.5 18.5 25.0 20.0 6.8 1.7 18.0 16.5 23.0 19.0 7.9 1.7 16.0 16.0 20.0 16.0 7.4 1.9 17.0 21.0 23.5 19.0 8.8 2.1 28.0 22.5 31.5 26.0 11.9 2.5 22.0 20.0 25.0 22.0 11.0 1.5 22.5 22.5 27.0 21.0 10.4 3.0 23.5 22.5 28.5 22.0 10.3 3.1 13.5 11.0 16.0 14.5 6.2 0.6 22.0 23.0 24.5 22.0 11.0 1.3 37.0 37.5 41.0 36.0 18.0 2.5 12.0 11.5 14.0 10.0 5.0 2.0 34.5 33.0 39.0 33.0 16.5 3.0 31.5 30.0 32.5 29.0 14.5 1.8 23.0 23.0 25.5 21.5 10.8 2.0 21.5 18.0 26.0 22.5 9.5 1.5 19.5 20.0 22.0 20.0 10.0 1.0 29.5 23.0 32.5 27.5 12.7 2.3 12.0 15.0 17.5 13.5 5.8 1.7 13.0 15.0 19.0 16.0 6.4 1.2 21.0 23.0 24.5 21.0 10.5 3.0 34.0 30.0 39.5 31.0 14.6 4.0 17.0 17.5 18.0 17.0 8.5 0.5 182 Table 43. Sample P27 Measurements crystal zone A. B C E size width 33.0 24.0 36.0 31.0 13.7 2.2 42.0 43.0 44.5 40.0 20.0 2.3 42.0 43.0 45.0 40.0 20.0 2.5 22.0 24.0 24.0 19.5 9.8 4.8 26.0 23.5 30.0 25.0 12.1 2.4 26.0 25.0 31.0 26.0 12.6 2.4 27.0 21.0 30.0 25.0 11.4 2.3 21.5 21.0 24.8 19.0 9.5 2.9 24.0 18.5 28.0 20.5 8.5 3.1 27.0 34.0 39.5 32.0 13.8 3.2 27.0 31.0 39.0 31.5 12.8 3.0 24.5 30.0 33.5 29.5 13.9 1.9 15.0 16.5 18.0 13.0 6.5 2.5 27.5 28.5 34.0 30.0 14.6 1.9 28.5 30.5 40.0 33.0 13.3 2.8 28.0 24.0 33.0 27.5 12.3 2.5 25.0 27.0 31.5 28.0 13.6 1.7 34.5 33.5 42.5 38.0 17.6 2.1 24.5 24.5 24.0 19.5 9.8 2.3 23.5 16.5 25.5 23.0 9.9 1.1 35.5 37.5 42.5 37.5 18.8 3.3 27.5 26.0 33.0 27.5 13.0 2.6 22.5 20.5 25.5 21.0 10.5 2.3 10.5 11.5 14.5 11.0 4.6 1.5 13.5 11.5 16.0 13.0 5.8 1.3 40.0 38.5 47.5 41.0 20.0 3.2 9.0 11.5 13.5 10.0 4.2 1.5 38.0 40.0 45.0 40.0 20.0 3.6 14.5 16.0 19.0 16.0 7.4 1.4 10.5 12.0 12.0 9.0 4.5 1.5 183 Table 44. Sample P31 Measurements crystal zone A B C E size width 21.0 21.5 25.5 19.0 9.4 3.2 27.5 24.0 32.0 25.5 11.9 3.0 23.0 23.0 27.5 25.0 12.4 1.2 24.5 25.5 30.5 26.0 12.5 2.2 10.0 11.0 12.5 11.5 5.8 0.5 25.5 25.5 28.0 25.5 12.8 1.3 16.0 14.5 16.0 12.5 6.3 1.8 25.0 24.5 28.0 23.5 11.8 2.3 25.0 25.0 27.5 25.0 12.5 1.3 16.0 20.0 22.0 20.0 9.5 0.9 20.0 19.0 23.0 21.0 10.5 1.0 15.0 15.0 18.0 16.0 7.9 1.0 27.5 33.5 40.0 36.0 15.2 1.7 37.0 35.0 41.5 34.5 17.3 4.6 27.5 33.0 40.0 35.0 14.6 2.1 17.5 16.5 19.5 17.0 8.5 1.3 26.5 22.0 30.5 28.5 12.9 0.9 26.0 26.5 33.5 27.5 12.3 2.7 27.5 26.0 29.5 25.5 12.8 2.0 13.5 10.0 14.5 13.0 6.0 0.7 22.0 26.0 29.5 25.0 11 8 2.1 19.0 21.0 25.0 23.0 10.6 0.9 23.0 23.5 29.5 25.5 11.5 1.8 12.5 14.0 15.0 13.0 6.5 1.0 18.0 17.0 20.5 18.5 9.3 1.0 21.0 20.5 24.5 21.0 10.5 1.8 28.0 32.0 38.5 35.0 15.5 1.5 27.0 30.0 35.0 32.5 15.5 1.2 18.5 17.5 20.0 19.5 9.8 0.3 22.5 25.0 29.0 26.0 12.5 1.4 24.0 23.0 25.0 23.0 11.5 1.0 184 Table 45. Sample P34 Measurements crystal zone .A B C E size width 30.0 22.0 32.0 26.0 12.0 2.8 31.0 25.0 35.0 31.5 14.4 1.6 31.0 30.0 35.0 29.0 14.5 3.0 27.0 23.0 31.5 25.0 11.4 3.0 27.0 23.0 30.0 24.0 11.8 2.9 30.0 24.5 38.5 31.0 11.4 2.8 18.0 20.0 24.5 19.0 8.3 2.4 27.0 31.0 43.0 39.0 13.1 1.3 13.5 14.5 15.5 12.5 6.3 1.5 20.5 19.0 24.0 22.0 10.7 1.0 43.0 34.0 60.0 54.5 16.1 1.6 19.5 27.0 32.0 24.5 9.3 2.9 21.0 25.5 29.0 25.0 11.5 1.8 20.0 24.0 27.5 21.5 9.9 2.8 13.5 13.0 15.5 13.5 6.8 1.0 13.0 16.5 18.5 12.0 5.4 2.9 19.5 20.0 24.0 17.0 8.3 3.4 20.0 20.0 24.0 16.5 8.2 3.7 13.5 17.0 19.5 16.5 7.2 1.3 42.0 43.5 53.0 42.5 20.0 4.9 17.5 23.0 25.0 22.0 10.2 1.4 26.0 23.5 31.0 23.5 10.8 3.5 29.5 22.0 32.0 25.0 11.4 3.2 21.5 23.5 26.0 23.0 11.5 2.1 17.5 19.5 21.5 18.0 9.0 2.1 35.5 35.0 34.0 28.5 14.3 2.8 21.0 20.5 22.0 19.0 9.5 1.5 25.5 34.5 43.0 30.0 10.6 4.6 18.0 18.5 21.0 17.5 8.8 1.8 12.5 11.0 12.0 8.5 4.3 1.8 185 ~.—r_’-. v0 .(\- 7. Table 46. Sample P36 Measurements crystal zone .A B C E size width 30.5 25.5 36.0 30.0 13.1 2.6 22.0 24.0 25.5 20.0 10.0 4.2 33.5 38.5 44.5 37.5 17.6 3.3 22.0 23.0 26.5 20.5 10.3 3.0 39.5 41.0 47.0 39.0 19.5 4.0 29.0 22.0 32.0 26.0 11.7 2.7 18.0 19.0 24.0 19.0 8.3 2.2 14.0 14.0 16.5 13.0 6.5 1.8 15.0 13.0 16.0 13.5 6.8 1.7 22.5 23.5 26.0 22.5 11.3 1.8 37.0 42.0 51.0 43.0 18.8 3.5 26.5 25.0 29.0 21.5 10.8 3.8 38.0 30.5 46.5 36.0 14.3 4.2 19.5 13.0 23.0 17.0 6.0 2.1 14.0 12.0 13.5 11.0 5.5 2.7 16.5 20.0 24.5 21.5 8.7 1.2 35.0 30.0 39.0 31.0 15.2 3.9 14.0 14.0 15.0 12.0 6.0 1.5 18.5 17.0 26.5 15.5 5.1 3.6 34.0 30.5 41.0 34.5 15.5 2.9 25.0 20.0 27.5 23.0 10.9 2.1 13.0 19.5 21.0 17.0 7.1 1.7 40.0 37.0 48.0 40.5 18.8 3.5 26.5 23.0 31.0 25.0 11.5 2.8 14.0 13.5 16.0 12.5 6.3 1.8 13.0 12.0 15.5 14.0 6.6 0.7 16.0 20.0 24.0 19.5 8.0 1.8 21.5 20.5 25.0 23.5 11.8 0.8 14.5 12.5 16.5 13.5 6.4 1.4 21.5 21.0 23.0 19.5 9.8 1.8 24.0 23.0 26.5 21.0 10.5 2.8 8.0 7.5 9.0 7.0 3.5 1.0 17.0 17.0 18.5 16.0 8.0 1.3 15.0 16.0 18.0 15.0 7.5 1.5 36.5 36.0 44.0 35.5 17.3 4.1 ’ 2€3.5 29.5 35.0 28.0 12.9 3.2 23.0 20.5 27.0 21.5 10.0 2.6 186 Table 46 (cont'd). crystal zone A B C 'E size width 28.5 27.5 34.5 26 12.3 4.0 20.0 22.0 26.5 20 9.1 3.0 187 Table 47. Sample P37 Measurements crystal zone A B C E size width 33.0 35.0 39.0 34.0 17.0 3.7 49.0 48.5 59.5 51.0 24.6 4.1 28.5 26.0 35.0 26.0 11.5 4.0 12.0 14.0 15.0 12.0 6.0 1.8 29.0 27.0 31.0 22.0 11.0 6.3 35.0 34.0 39.5 33.0 16.5 3.3 37.0 35.0 41.0 30.0 15.0 7.0 36.0 41.0 48.0 35.0 16.2 6.0 15.5 16.5 19.5 16.0 7.7 1.7 49.0 51.0 69.0 52.0 20.2 6.6 22.5 22.0 28 5 21.5 9.6 3.1 38.0 47.0 56.0 40.0 16.7 6.7 11.0 10.5 14.0 6.0 2.6 3.5 52.0 35.0 55.0 39.0 16.9 6.9 28.0 28.0 32.5 23.0 11.5 4.8 27.0 23.0 31 5 26.0 11.8 2.5 48.5 42.0 55.0 40.0 19.3 7.2 28.0 26.0 32.0 25.0 12.5 3.6 28.5 27.5 33.0 26.0 13.0 3.5 54.0 52.0 57.0 52.0 26.0 7.2 40.0 44.0 52.0 44.0 20.7 3.8 15.0 13.5 16.5 14.0 7.0 1.3 24.0 24.0 25.0 21.0 10.5 2.0 27.0 24.0 32.0 20.0 9.2 5.5 25.5 22.0 31.0 24.0 10.3 3.0 13.0 15.0 18.0 14.0 6.2 1.8 8.0 8.0 10.5 7.5 3.2 1.3 8.0 9.5 10 0 6.0 3.0 2.0 12.0 10.0 12.5 8.0 4.0 2.6 18.0 20.5 24.0 17.5 8.1 3.0 22.0 21.5 22.0 16.0 8.0 3.0 18.0 18.5 20.0 13.0 6.5 3.5 17.0 16.0 20.5 14.0 6.6 3.0 35.5 43.0 49.0 34.5 15.8 6.7 21.0 22.0 22.0 15.5 7.8 3.3 14.0 14.5 18.0 13.0 5.9 2.3 24.5 24.0 28.5 17.5 8. 5.5 188 Table 48. Sample P40 Measurements crystal zone .A B C E size width 18.5 13.5 20.0 15.5 7.0 2.0 11.0 10.5 10.0 9.0 4.5 0.5 15.5 13.5 18.0 15.0 7.0 1.4 18.0 17.0 19.0 14.5 7.3 2.3 18.5 20.0 24.0 18.5 8.6 2.6 15.5 16.0 18.0 14.5 7.3 1.8 18.0 15.0 20.0 17.0 8.2 1.4 25.0 30.0 33.5 28.5 13.6 2.4 13.0 15.0 18.5 15.5 6.5 1.3 17.5 23.5 25.5 20.0 9.1 2.5 16.0 14.5 17.5 15.5 7.8 1.0 24.0 30.5 35.5 29.0 12.3 2.8 22.0 27.5 30.0 22.0 10.5 3.8 26.0 25.5 27.0 22.0 11.0 2.5 25.5 25.5 30.0 25.0 12.5 2.5 19.0 18.0 23.0 16.0 7.5 3.3 17.5 11.5 19.5 15.0 5.8 1.8 21.5 21.0 24.5 21.0 10.5 1.8 14.5 14.0 16.5 12.5 6.3 2.0 12.5 13.0 15.0 10.0 5.0 2.5 10.0 12.0 12.5 8.5 4.3 2.4 15.5 18.5 20.5 13.5 6.6 3.4 16.5 12.0 19.0 15.0 6.1 1.6 19.2 19.5 23.5 17.5 8.5 2.9 15.5 15.5 18.5 14.0 7.0 2.2 14.5 13.0 17.5 14.0 6.3 1.6 14.5 13.5 17.5 14.5 6.7 1.4 9.0 14.0 15.0 10.0 4.1 2.0 23.0 21.0 24.0 18.0 9.0 4.6 24.0 17.5 26.0 19.5 8.7 2.9 33.0 27.5 38.5 30.0 13.4 3.8 16.5 18.5 20.0 15.5 7.8 2.9 29.0 34.0 38.5 32.0 15.3 3.1 22.5 23.5 24.5 20.5 10.3 2.0 189 3.96,. _ 1:37" T's") 4. ' Table 49. Sample P41 Measurements crystal zone A. B C E size width 15.5 15.0 18.5 14.0 6.8 2.2 10.0 11.0 13.0 11.5 5.4 0.7 25.0 23.0 28.5 23.0 11.5 2.8 25.0 29.5 38.0 31.0 11.8 2.7 21.0 26.0 29.0 22.5 10.5 3.0 32.5 40.0 55.5 42.5 13.1 4.0 25.5 21.5 28.5 20.5 9.9 3.9 34.0 38.5 43.5 36.5 18.0 3.4 12.0 11.0 13.0 10.0 5.0 1.5 16.5 16.5 20.5 14.5 6.8 2.8 17.0 20.5 23.5 20.0 9.1 1.6 19.5 19.5 23.5 19.5 9.6 2.0 24.5 22.5 27.0 20.0 10.0 4.2 12.0 20.0 20.5 16.0 6.6 1.8 16.5 16.5 19.5 16.5 8.3 1.5 11.5 12.0 13.5 11.0 5.5 1.3 12.5 20.0 20.5 17.0 7.2 1.5 28.0 31.0 36.5 30.5 14.3 2.8 24.0 25.5 29.5 22.0 11.0 3.8 22.5 24.0 28.0 22.0 10.8 2.9 29.5 26.5 35.5 28.0 12.6 3.4 25.0 28.5 33.0 24.5 11.5 4.0 15.5 14.0 15.5 10.5 5.3 2.5 29.0 28.0 35.0 25.0 11.9 4.8 29.0 32.0 40.5 31.0 12.9 4.0 16.5 14.5 18.5 15.0 7.5 1.7 15.0 14.0 16.0 11.0 5.5 2.5 11.0 11.5 13.5 8.0 4.0 2.7 20.5 22.0 24.5 20.0 10.0 2.3 28.0 29.0 32.5 23.5 11.8 4.5 13.5 13.5 16.5 11.0 5.3 2.6 17.5 17.5 19.0 13.0 6.5 3.0 33.0 28.5 37.0 28.5 13.9 4.2 22.5 20.5 26.5 23.5 11.1 1.4 19.0 20.5 23.0 18.0 9.0 2.5 25.5 23.5 26.0 18.0 9.0 6.4 190 Table 50. Sample P45 Measurements crystal zone A B C E size width 16.5 16.5 20.0 15.0 7.3 2.4 24.0 23.0 24.0 18.0 9.0 3.0 26.5 23.0 34.5 27.0 10.3 2.9 20.5 18.5 23.5 19.0 9.3 2.2 16.0 15.0 16.5 13.5 6.8 1.5 13.5 11.5 14.5 11.5 5.8 1.7 35.5 35.5 41.5 36.0 18.0 2.8 33.0 34.0 47.0 40.0 15.1 2.6 14.0 16.0 19.0 14.5 6.5 2.0 22.0 19.0 26.0 20.0 9.0 2.7 24.8 23.5 29.0 24.0 11.9 2.5 28.5 23.5 33.0 26.5 11.8 2.9 20.5 21.5 24.5 20.0 10.0 2.3 24.0 22.0 27.5 23.0 11.4 2.2 28.0 26.0 35.0 22.0 9.6 5.7 41.5 34.0 47.0 39.0 18.0 3.7 16.0 14.0 17.5 15.5 7.8 1.2 26.5 28.0 35.0 27.0 12.0 3.5 12.5 14.0 18.0 13.0 5.2 2.0 27.0 28.0 35.0 28.0 12.6 3.1 7.5 8.0 9.5 7.5 3.6 1.0 21.0 19.5 25.5 18.5 8.5 3.2 22.0 24.0 28.0 23.0 11.1 2.4 29.0 24.0 32.5 24.0 11.3 4.0 27.0 26.0 35.0 24.0 10.1 4.6 41.0 35.0 47.0 38.0 17.8 4.2 21.0 20.5 22.5 19.0 9.5 1.8 13.5 19.0 20.5 10.0 4.4 4.6 12.0 9.5 13.0 10.5 5.0 1.2 24.0 22.5 28.0 21.5 10.6 3.2 27.5 26.5 32.5 22.0 10.8 5.2 13.5 15.5 17.0 12.0 6.0 2.7 23.5 27.0 33.5 27.5 11.5 2.5 191 Table 51. Sample List for Saluda Formation Hwy 7 and Hwy 56 Outcrops 192 Table 52. Sample Sal R-l Measurements crystal zone A B C E size width 17.0 16.0 19.0 15.0 7.5 2.0 25.5 32.0 36.0 30.0 13.6 2.7 28.0 28.0 30.5 25.0 12.5 2.8 32.0 24.5 36.0 33.0 14.5 1.3 31.0 25.0 34.5 29.5 13.8 2.3 13.0 16.0 18.0 16.5 7.6 0.7 8.0 8.0 9.5 8.0 4.0 0.8 10.5 11.0 13.0 12.0 5.9 0.5 17.5 19.5 23.0 18.0 8.4 2.3 26.0 23.0 30.0 23.0 11.0 3.3 9.5 10.5 13.0 10.5 4.5 1.1 21.0 21.0 25.0 21.0 10.5 2.0 28.0 25.5 33.0 22.5 10.6 5.0 35.0 32.0 40.5 33.0 16.1 3.7 32.0 34.0 39.0 29.0 14.5 5.2 23.0 19.5 26.5 20.0 9.2 3.0 25.5 25.5 31.0 23.5 11.4 3.6 34.0 35.0 40.5 33.5 16.8 3.5 27.5 19.5 29.0 24.0 10.9 2.3 22.0 22.5 26.0 22.0 11.0 2.0 11.5 9.5 12.5 9.0 4.5 1.7 22.5 21.0 26.0 15.5 7.7 5.2 39.0 39.5 53.5 45.5 18.1 3.2 27.0 19.5 29.0 20.5 9.2 3.8 27.0 24.0 32.0 27.0 12.4 2.3 25.0 18.5 29.0 21.5 8.7 3.0 22.5 21.5 26.0 19.5 9.8 3.3 34.0 32.0 36.5 31.0 15.5 4.9 21.0 15.0 23.0 16.0 6.9 3.0 25.5 24.5 30.5 22.0 10.6 4.1 11.5 16.5 20.0 15.0 5.3 1.8 33.5 34.5 39.5 30.0 15.0 4.8 22.5 19.5 26.0 21.5 10.1 2.1 24.0 24.5 29.5 23.0 11.1 3.1 26.0 19.5 29.5 23.5 10.0 2.6 21.5 22.5 25.5 21.0 10.5 2.3 18.5 20.5 21.5 15.5 7.8 4.3 193 Table 53. Sample Sal R-5 Measurements crystal zone A B C E size width 16.0 19.0 22.0 17.0 7.7 2.3 18.0 16.0 23.0 18.0 7.2 2.0 19.0 18.0 21.0 16.5 8.3 2.3 28.0 31.0 40.5 27.0 10.6 5.3 28.0 43.0 45.5 35.5 14.9 4.2 14.5 15.5 18.0 13.0 6.4 2.5 21.0 20.0 22.0 16.5 8.3 2.8 17.5 18.0 20.0 18.0 9.0 1.0 16.0 16.0 18.0 14.0 7.0 2.0 18.0 17.5 19.0 15.0 7.5 2.0 8.5 10.0 11.5 9.0 4.2 1.2 17.0 18.0 19.0 15.0 7.5 2.0 21.0 24.0 28.0 24.5 11.4 1.6 13.0 15.0 16.0 14.0 7.0 1.5 16.0 17.5 21.0 16.0 7.4 2.3 27.0 27.5 29.0 26.0 13.0 1.5 21.0 20.5 25.0 20.5 10.1 2.2 21.5 21.5 24.5 19.0 9.5 2.8 21.5 20.5 23.5 16.0 8.0 3.8 16.5 19.0 22.0 20.0 9.3 0.9 27.0 27.5 31.0 26.5 13.3 2.3 24.5 18.0 26.0 21.5 10.0 2.1 30.0 26.0 34.5 29.0 13.7 2.6 16.5 15.0 17.5 15.0 7.5 1.3 25.0 23.5 32.5 24.5 10.1 3.3 14.5 14.5 16.0 11.5 5.8 2.3 23.0 31.0 35.0 24.5 10.4 4.5 21.0 19.5 27.0 17.0 7.0 4.1 28.0 27.5 36.0 28.0 12.2 3.5 26.5 24.0 31.0 25.5 12.1 2.6 36.0 34.0 38.0 30.5 15.3 6.5 19.0 16.5 23.0 21.0 9.1 0.9 30.0 26.0 37.0 29.5 12.4 3.1 194 Table 54. Sample Sal R-lO Measurements crystal zone A B C E size width 16.0 17.0 21.0 18.0 8.1 1.3 17.0 18.0 18.5 16.0 8.0 1.3 20.5 22.0 25.0 21.0 10.5 2.0 22.0 16.0 25.5 21.0 8.4 1.8 23.0 19.5 26.5 23.0 10.6 1.6 10.0 11.0 12.0 10.0 5.0 1.0 36.0 34.0 41.0 37.0 18.5 2.5 16.5 19.0 22.0 19.0 8.9 1.4 30.5 33.0 41.0 33.0 14.5 3.5 28.5 28.0 35.5 26.0 12.0 4.4 35.0 36.0 44.0 41.0 19.3 1.4 33.5 33.5 41.0 37.0 17.8 1.9 10.0 9.5 10.5 7.5 3.8 1.5 31.0 33.5 39.0 33.5 16.4 2.7 28.5 29.0 32.0 27.5 13.8 2.3 15.0 19.0 21.0 13.5 6.3 3.5 32.5 35.0 41.5 36.0 17.1 2.6 28.5 30.0 31.0 25.0 12.5 3.0 31.5 26.0 35.0 27.5 13.1 3.6 21.0 25.5 28.0 23.0 11.2 2.4 21.0 21.0 24.0 17.5 8.8 3.3 40.0 41.5 49.0 42.0 20.7 3.5 17.0 17.5 21.0 16.0 7.7 2.4 32.0 21.5 34.5 30.0 12.6 1.9 27.0 27.0 33.5 27.0 12.7 3.1 40.5 42.0 51.0 40.0 18.9 5.2 25.5 22.0 29.5 26.5 12.3 1.4 45.0 47.0 52.5 44.0 22.0 6.0 28.5 30.5 29.0 26.0 13.0 6.0 40.0 38.0 39.0 32.0 16.0 9.1 195 Table 55. Sample Sal D-25 Measurements crystal zone A B C E size width 26.5 18.0 27.5 22.5 10.1 2.2 24.0 29.5 34 0 28.5 12.7 2.4 17.0 16.5 19.0 17.0 8.5 1.0 41.0 38.0 47.5 38.0 18.7 4.7 26.5 24.5 31.0 24.5 11.9 3.1 18.0 16.0 20.0 16.5 8.3 1.9 41.5 48.0 54.0 45.0 21.9 4.4 21.0 19.0 24.5 20.0 9.6 2.1 21.0 22.5 25.0 22.5 11.3 1.3 27.5 28.0 29.0 25.5 12.8 1.8 12.5 14.0 16.0 13.5 6.6 1.2 21.5 21.0 28.5 25.0 10.3 1.4 26.0 24.0 30.0 25.5 12.6 2.2 13.0 14.5 16.5 14.0 6.9 1.2 28.0 29.0 33.0 30.0 15.0 1.5 25.5 22.5 30.0 23.0 10.6 3.2 25.5 16.5 27.0 21.0 8.8 2.5 19.5 22.0 25.0 20.5 10.0 2.2 22.0 22.0 25.5 21.5 10.8 2.0 15.5 14.0 19.0 16.5 7.3 1.1 31.5 30.0 41.0 33.5 13.9 3.1 39.5 37.5 44.0 39.0 19.5 3.9 34.0 28.5 38.0 31.5 15.1 3.1 19.5 24.5 27.0 20.5 9.6 3.1 24.0 23.5 32.0 28.5 11.6 1.4 21.0 22.0 25.0 20.5 10.3 2.3 16.5 18.5 19.0 14.0 7.0 3.9 9.0 8.5 11.5 7.0 3.0 1.9 26.0 18.0 27.5 21.5 9.5 2.7 24.0 23.5 28.0 26.5 13.3 0.8 196 Table 56. Sample Sal D-34 Measurements crystal zone A B C E size width 16.0 19.5 22.0 17.5 8.1 2.1 33.5 36.0 43.0 34.5 16.2 4.0 34.0 35.5 48.0 38.0 14.8 3.9 20.5 20.0 27.0 21.5 8.9 2.3 22.5 22.0 26.0 22.0 11.0 2.0 53.0 49.0 68.5 51.0 20.9 7.2 34.0 35.0 39.5 29.0 14.5 5.3 26.0 17.0 27.5 22.5 9.5 2.1 29.5 26.0 37.0 34.0 14.1 1.2 13.0 11.5 14.5 9.0 4.5 2.8 14.5 13.0 16.0 11.5 5.8 2.3 25.5 24.0 29.0 24.0 12 0 2.5 25.5 35.5 38.5 33.0 14 5 2.4 14.0 14.5 18.5 18.0 7.8 0.2 25.5 35.0 40.5 33.0 13.2 3.0 33.0 23.0 37.5 29.5 11.7 3.2 20.0 20.0 23.0 14.5 7.3 4.3 44.5 42.0 56.5 45.5 19.6 4.7 21.0 32.0 34.0 23.5 9.9 4.4 39.0 40.0 48.0 37.5 18.2 5.1 21.0 15.5 25.0 19.0 7.3 2.3 39.0 42.5 49.5 43.0 20.8 3.1 20.0 18.0 32.0 26.0 6.2 1.4 21.5 23.0 31.0 23.0 8.8 3.1 32.5 32.0 36.5 32.5 16 3 2.0 35.0 34.0 41.0 32.0 16 0 4.5 47.0 49.0 58.5 50.0 24 1 4.1 39.0 39.0 46.0 38.5 19 3 3.8 16.0 16.0 19.0 15.5 7.8 1.8 15.5 13.5 17.0 12.5 6.3 2.4 197 Table 57. Sample Sal A-ld Measurements crystal zone .A B C E size width 19.5 20.0 21.0 17.5 8.8 1.8 28.5 23.5 32.5 26.0 11.9 3.0 21.5 22.0 24.0 18.5 9.3 2.8 48.5 41.0 56.0 46.0 21.1 4.6 31.5 30.5 37.5 30.0 14.7 3.7 29.5 22.0 32.0 27.0 12.3 2.3 36.0 23.0 45.0 30.5 9.2 4.4 24.5 19.0 29.0 22.0 9.0 2.9 21.5 20.0 25.0 19.0 9.3 2.9 27.0 25.0 31.0 24.0 12.0 3.5 30.5 32.0 37.0 25.0 12.5 6.0 19.5 24.0 29.5 24.0 9.5 2.2 28.0 17.0 29.0 25.0 10.2 1.6 22.0 14.0 24.5 18.0 6.8 2.5 15.0 14.0 16.5 11.0 5.5 2.8 15.0 19.0 22.0 15.5 6.7 2.8 22.0 28.0 35.0 25.5 9.5 3.5 25.5 23.0 33.5 26.0 10.1 2.9 49.5 33.0 53.0 40.0 16.8 5.5 18.0 16.5 20.0 17.0 8.5 1.5 24.5 16.5 28.0 20.0 7.6 3.0 20.0 24.5 31.5 26.0 9.5 2.0 20.5 24.5 32.0 27.0 9.8 1.8 19.0 17.0 20.0 16.5 8.3 2.8 12.5 11.0 13.5 11.0 5.5 1.3 19.5 21.0 20.0 15.5 7.8 2.3 16.0 16.0 22.0 18.0 7.1 1.6 20.5 20.5 24.0 20.5 10.3 1.8 22.0 28.0 33.5 24.0 9.7 3.8 19.5 15.5 24.5 21.5 8.0 1.1 31.0 24.5 36.0 30.0 12.9 2.6 8.0 12.0 14.5 10.0 3.4 1.5 198 Table 58. Sample Sal A—5d Measurements crystal zone A B C E size width 32.0 31.5 32.0 31.0 15.5 0.5 11.0 11.0 12.0 9.5 4.8 1.3 11.5 10.5 12.5 11.0 5.5 0.8 17.0 19.0 20.0 17.0 8.5 2.6 12.0 12.5 15.5 12.5 5.7 1.4 26.5 25.0 32.5 26.5 12.1 2.7 20.0 20.0 23.0 19.0 9.5 2.0 17.0 15.0 20.0 16.5 7.6 1.6 37.5 33.5 42.5 40.0 19.8 1.2 16.0 15.0 19.0 15.5 7.4 1.7 10.5 14.5 16.0 13.5 5.8 1.1 25.0 23.5 28.0 25.5 12.8 1.3 15.5 16.0 18.0 16.5 8.3 0.8 23.0 25.0 27.0 22.5 11.3 3.4 34.0 38.0 44.5 41.0 19.3 1.6 17.5 18.0 24.0 20.0 8.1 1.6 20.0 18.0 23.0 19.5 9.5 1.7 51.0 49.0 64.0 50.0 22.3 6.2 31.0 34.0 41.0 33.5 15.3 3.4 18.0 16.0 24.5 18.0 6.4 2.3 31.0 34.5 42.0 34.0 15.1 3.5 19.5 20.0 25.5 19.5 8.6 2.6 16.5 17.0 21.5 16.0 7.1 2.4 17.0 23.0 28.0 23.5 8.7 1.7 19.5 19.0 26.0 20.5 8.3 2.2 31.0 34.5 41.0 34.0 15.7 3.2 29.5 36.0 43.0 34.0 14.3 3.8 24.5 19.5 28.5 19.5 8.4 3.9 18.5 18.5 20.5 16.0 8.0 2.3 16.0 17.0 22.5 16.5 6.6 2.4 199 Table 59. Sample Sal A-7d Measurements crystal zone A B C E size width 29.0 24.0 32.5 28.0 13.2 2.1 16.5 21.5 24.5 18.5 8.0 2.6 26.0 22.0 29.0 22.5 10.9 3.2 32.0 28.0 36.0 27.5 13.5 4.2 23.5 16.0 26.0 20.0 8.1 2.4 29.0 28.0 32.0 26.5 13.3 2.8 16.0 16.5 19.0 14.0 7.0 2.5 15.5 20.5 22.0 18.5 8.7 1.6 23.5 23.0 28.0 23.0 11.3 2.5 38.0 38.0 44.0 35.5 17.8 4.3 28.5 28.5 31.5 26.0 13.0 2.8 19.5 18.0 22.0 18.0 9.0 2.0 28.0 32.0 37.0 29.0 13.7 3.8 20.5 13.5 22.0 16.5 6.8 2.3 16.0 15.5 18.5 15.0 7.5 1.8 26.0 25.5 32.0 25.5 11.9 3.0 26.0 23.0 31.5 23.0 10.1 3.7 12.5 14.0 15.5 12.5 6.3 1.5 25.0 21.5 28.0 23.5 11.5 2.2 16.0 18.0 18.5 13.5 6.8 3.8 15.5 17.5 19.5 16.5 8.3 1.6 30.0 29.5 33.0 24.5 12.3 4.3 20.0 21.0 25.0 18.0 8.7 3.4 22.5 21.5 23.5 18.5 9.3 2.5 30.0 32.0 37.0 29.0 14.5 3.9 11.5 14.5 16.0 11.0 5.1 2.3 32.5 36.0 41.0 33.0 16.3 4.0 16.5 16.0 20.5 17.0 7.8 1.6 17.5 19.0 21.5 17.0 8.5 2.3 20.5 30.0 37.5 29.0 9.4 2.8 24.5 24.0 28.5 25.0 12 5 1.8 36.5 35.0 39.0 32.5 16 3 3.3 30.0 22.0 32.0 26.0 12.0 2.8 17.0 20.0 24.0 16.5 7.1 3.2 19.5 18.0 23.0 17.5 8.4 2.6 36.5 37.5 40.5 31.5 15.8 4.5 17.0 16.0 20.0 16.5 8.0 1.7 200 Table 59 (cont'd). crystal zone A B C E size width 25.0 20.0 27.5 22.0 10.4 2.6 28.0 25.0 32.0 24.0 11.7 3.9 28.5 28.0 34.0 28.5 14.0 2.7 28.0 27.0 32.0 26.0 13.0 3.0 31.0 25.0 36.0 30.0 13.1 2.6 36.0 35.0 42.5 33.5 16.6 4.5 31.0 32.0 41.0 33.0 14.3 3.5 36.0 31.0 43.0 33.5 14.8 4.2 201 Table 60. Sample Sal A-5g Measurements crystal zone A B C E size width 9.5 11.5 13.5 12.5 5.5 0.4 37.5 34.5 45.5 37.5 17.0 3.6 24.0 26.0 28.5 20.5 10.3 5.0 39.0 35.0 46.0 36.0 16.8 4.7 13.5 8.5 14.5 9.5 3.8 2.0 43.5 42.0 53.0 43.0 20.2 4.7 14.5 16.5 17.0 12.5 6.3 3.3 13.0 15.0 15.5 11.0 5.5 3.1 32.5 35.5 41.0 35.0 17.2 2.9 29.0 30.5 35.0 29.0 14.5 3.0 49.0 50.0 61.0 49.0 23.3 5.7 15.0 15.0 15.5 11.5 5.8 2.0 30.5 29.5 27.5 22.0 11.0 2.8 49.5 50.5 62.0 49.0 23.0 6.1 17.5 17.0 20.0 14.5 7.3 2.8 44.0 45.5 45.5 38.5 19.3 3.5 17.5 17.5 19.0 15.0 7.5 2.0 27.0 26.5 33.0 23.0 10.9 4.7 10.5 12.5 13.0 9.5 4.8 2.2 25.5 22.5 32.0 24.0 9.9 3.3 18.0 22.5 26.0 22.0 9.6 1.7 34.5 39.0 47.0 33.0 14.7 6.2 33.0 35.0 41.0 35.0 17.2 2.9 29.0 39.0 47.5 31.5 11.7 5.9 19.0 16.5 22.0 16.0 7.5 2.8 15.5 17.0 21.0 15.5 6.8 2.4 10.0 16.5 17.0 13.5 5.5 1.4 18.0 19.5 22.5 20.0 9.9 1.2 27.0 27.0 36.0 28.0 11.6 3.3 28.0 27.5 35.0 30.0 13.7 2.3 202 Table 61. Sample Sal Ar7g Measurements crystal zone A. B C E size width 19.5 17.0 22.0 19.5 9.5 1.2 33.0 32.0 44.0 29.5 11.9 5.9 18.5 17.0 21.5 18.0 8.8 1.7 10.0 12.0 12.0 9.5 4.8 2.0 9.5 9.0 12.0 9.5 4.1 1.1 15.0 17.0 20.0 19.0 8.8 0.5 17.5 18.5 19.5 16.5 8.3 1.5 11.5 13.5 12.5 11.0 5.5 2.4 28.0 28.5 33.0 28.5 14.3 2.3 11.0 10.5 13.0 11.5 5.6 0.7 17.0 17.5 19.0 14.0 7.0 2.5 30.5 30.5 35.0 28.5 14.3 3.3 20.5 21.0 24.0 20.5 10.3 1.8 17.5 16.5 20.0 17.5 8.8 1.3 12.0 10.0 12.5 11.0 5.5 1.1 24.0 19.0 29.0 24.5 9.8 1.8 14.5 15.5 17.0 15.5 7.8 0.8 13.0 12.0 14.0 13.0 6.5 0.5 29.5 23.5 32.0 28.5 13.7 1.7 21.0 21.0 24.5 18.5 9.3 3.0 18.5 19.0 23.0 18.5 8.8 2.2 11.5 12.5 16.5 12.5 4.9 1.6 21.5 21.0 24.5 19.5 9.8 2.5 26.0 25.0 30.5 27.0 13.4 1.7 21.0 24.0 28.0 23.0 10.7 2.3 25.5 22.5 29.5 23.5 11.1 2.8 28.5 32.0 39.0 36.5 16.0 1.1 12.0 12.0 14.5 12.5 6.1 1.0 20.0 21.0 23.0 19.0 9.5 2.0 21.0 19.0 23.0 20.5 10.3 1.9 203 Table 62. Sample Sal 56-1 Measurements crystal zone A B C E size width 27.5 29.0 31.0 24.5 12.3 3.3 26.5 24.5 31.0 26.0 12.6 2.4 26.0 22.5 .0 25.0 11.7 2.3 37.5 30.5 5 40.5 15.9 2.4 14.5 16.5 .5 15.0 6.3 2.3 16.0 17.5 .5 15.0 7.5 2.3 44.0 49.0 .0 48.5 21.9 4.7 19.0 18.5 .0 15.0 7.5 3.0 24.5 17.0 .0 21.5 9.5 2.0 10.0 11.0 .0 9.5 4.8 1.3 20.5 22.5 .0 21.5 10.5 2.2 26.5 30.5 .0 28.0 13.3 3.3 23.5 27.0 .5 22.5 11.0 3.9 13.5 13.0 .0 12.0 5.9 2.0 9.5 10.0 .0 9.5 3.9 1.5 13.5 16.5 .0 16.5 5.6 1.9 17.5 17.0 .5 17.5 7.6 2.2 23.0 27.5 .5 25.0 11.5 3.0 38.5 40.0 .0 41.0 17.2 4.6 48.0 37.5 .0 45.0 18.9 4.6 27.0 27.0 .0 27.0 13.5 2.5 13.5 15.0 .5 13.5 6.4 1.9 19.0 18.5 .5 18.5 9.3 1.5 31.0 35.5 .0 34.5 16 9 2.7 12.0 10.5 .0 10.5 5.3 1.3 27.5 28.0 .0 23.5 11.3 5.0 13.5 15.0 .5 12.0 6.0 1.8 28.0 28.0 .5 29.5 14.0 2.4 32.0 29.0 .0 33.0 16.0 1.9 9.0 11.0 .0 11.0 5.5 0.4 22.5 25.0 .0 26.0 10.0 2.7 204 Table 63. Sample Sal 56-5 Measurements crystal zone .A B C E size width 22.5 15.0 28.0 14.0 4.5 4.5 40.0 38.0 46.0 40.0 20.0 3.4 14.5 15.0 19.0 12.0 5.3 3.1 19.0 18.5 22.5 13.0 6.4 4.7 40.0 40.0 48.0 30.0 14.9 8.9 22.0 16.0 27.0 14.0 5.0 4.7 30.0 31.0 39.0 28.5 12.7 4.7 16.5 17.0 20.0 10.0 5.0 5.0 25.5 29.0 34.5 23.0 10.4 5.2 29.5 27.5 38.5 21.0 8.5 7.1 8.5 10.0 12.0 8.0 3.5 1.7 12.0 12.0 15.5 8.5 3.7 3.1 30.0 26.0 38.5 31.0 12.1 2.9 22.5 20.0 27.5 22.0 9.6 2.4 23.5 27.0 34.5 26.0 10.3 3.4 14.5 15.0 17.0 13.5 6.8 1.8 29.0 25.5 34.5 20.0 9.0 6.6 11.0 10.5 13.5 8.5 3.9 2.3 10.5 10.0 12.0 8.5 4.3 1.8 31.0 38.0 42.0 32.0 15.3 4.8 7.5 6.5 8.5 5.0 2.4 1.7 24.0 24.5 34.0 27.0 10.2 2.6 24.0 23.0 26.5 20.0 10.0 3.3 16.5 19.0 23.0 12.0 5.2 4.8 25.0 28.0 32.0 24.0 11.7 3.9 23.0 20.5 26.5 21.5 10.3 2.4 25.0 18.5 32.5 23.5 7.6 2.9 24.5 26.5 31.5 26.5 12.5 2.4 23.0 22.0 28.5 23.0 10.4 2.5 17.5 16.0 20.0 11.0 5.5 4.5 205 w . "-3.1?" 7 . k‘r.. Table 64. Sample Pay-1 Measurements crystal zone A. B C E size width 11.5 9.0 14.0 12.0 4.7 0.8 12.5 15.0 17.0 15.5 7.2 0.7 18.0 17.0 22.0 19.0 8.7 1.4 26.0 32.5 36.0 30.5 14.3 2.6 19.5 19.0 22.5 20.5 10.3 1.0 10.5 11.0 12.5 10.0 5.0 1.3 28.0 26.0 32.0 28.0 14.0 2.1 15.0 15.5 20.0 18.0 7.7 0.9 26.5 20.5 28.5 25.0 11.9 1.7 30.5 26.5 35.0 31.0 14.7 1.9 29.5 21.0 34.0 28.0 11.1 2.4 18.5 17.5 21.5 18.5 9.2 1.5 15.5 15.5 18.0 15.5 7.8 1.3 45.0 37.0 52.0 46.0 20.6 2.7 13.0 14.5 15.5 13.0 6.5 1.3 15.5 15.5 18.5 15.5 7.7 1.5 28.0 27.5 30.0 26.0 13.0 2.0 21.5 30.5 32.0 27.5 12.6 2.1 10.0 9.0 12.0 9.5 4.3 1.1 19.0 19.0 20.0 17.5 8.8 1.3 18.5 18.5 24.5 21.5 9.0 1.3 17.5 17.5 21.5 18.0 8.6 1.7 15.5 18.0 22.0 19.5 8.3 1.1 19.0 19.0 23.0 20.0 9.8 1.5 24.0 18.0 27.5 24.5 10.2 1.3 17.5 18.0 21.5 17.5 8.5 2.0 18.0 21.5 24.0 22.5 10.8 0.7 22.5 24.5 25.5 22.0 11.0 3.6 14.5 12.5 15.5 14.0 7.0 1.1 24.0 23.5 29.0 24.5 11.8 2.2 206 Table 65. Sample Pay-5 Measurements crystal zone A B C E size width 31.0 34.0 42.0 34.5 15.1 3.3 12.0 13.0 15.0 11.0 5.4 2.0 19.5 20.0 23.5 20.5 10.3 1.5 37.0 36.0 44.0 33.5 16.5 5.2 22.0 18.0 24.5 22.0 10.4 1.2 14.0 12.5 15.0 11.5 5.8 1.8 21.0 21.0 24.5 20.0 10.0 2.3 18.0 19.0 23.0 18.5 8.6 2.1 25.0 22.0 33.5 27.0 9.8 2.4 14.0 10.5 15.5 13.0 5.8 1.1 18.0 21.5 27.0 22.5 8.8 1.8 18.5 21.5 25.5 23.0 10 3 1.1 10.0 12.5 14.0 12.5 5.7 0.7 11.5 12.5 14.5 13.0 6.4 0.7 35.0 34.0 44.5 37.0 16.3 3.3 10.0 12.0 14.0 11.5 5.1 1.1 17.0 16.5 17.5 16.5 8.3 0.5 13.0 11.0 14.5 13.0 6.3 0.7 15.5 15.5 18.5 17.5 8.7 0.5 20.5 19.0 23.0 20.0 10 0 1.5 29.0 37.5 47.0 37.0 13.5 3.7 26.0 25.0 26.0 21.0 10.5 2.5 22.0 23.0 27.0 25.0 12.4 1.0 27.0 24.0 31.0 26.0 12.6 2.4 17.0 19.0 22.0 20.0 9.6 1.0 20.0 19.0 21.5 18.0 9.0 1.8 46.0 42.0 56.0 50.0 22.4 2.7 13.5 15.5 17.5 14.0 6.8 1.7 15.0 14.0 18.5 16.0 7.2 1.1 18.0 15.0 21.5 18.5 7.9 1.3 20.5 22.0 26.0 22.0 10.5 1.9 26.0 26.5 31.5 29.0 14.4 1.2 24.5 26.0 30.0 27.0 13.5 1.5 16.0 14.0 18.5 14.5 6.8 1.9 207 I! Table 66. Sample Pay-11 Measurements crystal zone A B C E size width 15.0 13.0 19.0 16.0 6.4 1.2 19.0 20.0 24.5 23.0 10.6 0.7 8.5 6.5 9.0 8.0 4.0 0.3 20.5 18.5 24.0 21.5 10.2 1.2 31.5 33.0 36.5 30.0 15.0 3.3 17.5 17.5 21.0 19.5 9.7 0.7 8.0 7.5 8.5 7.5 3.8 0.5 10.0 10.0 11.5 10.0 5.0 0.8 36.5 33.0 45.0 36.0 15.7 3.9 24.0 23.5 30.0 26.0 11.9 1.8 20.0 19.0 25.5 19.5 8.4 2.6 25.0 25.0 27.5 23.5 11.8 2.0 18.0 16.0 21.5 19.0 8.6 1.1 13.0 13.0 15.5 13.0 6.5 1.3 13.0 13.0 15.0 12.5 6.3 1.3 15.0 13.5 16.5 15.0 7.5 0.8 23.5 21.5 24.0 21.0 10.5 3.6 22.5 23.0 24.5 21.0 10.5 1.8 30.5 41.0 48.0 39.5 15.8 3.4 22.0 24.0 30.0 25.0 10.8 2.2 32.5 24.0 35.0 30.0 13.7 2.3 31.5 31.0 35.0 31.5 15.8 1.8 20.0 20.0 25.0 22.5 10.4 1.2 19.0 19.0 21.0 17.5 8.8 1.8 20.0 20.5 23.5 22.5 11.3 0.5 27.0 29.5 36.0 31.5 .1 2.0 12.0 11.0 13.0 12.0 .0 0.5 20.0 15.5 23.5 19.5 8.0 1.7 20.0 18.5 24.0 22.0 10.2 0.9 40.0 43.5 53.0 44.0 19.8 4.1 208 Table 67. Sample Ton—11 Measurements crystal zone A B C E size width 22.5 21.0 24.0 21.5 10.8 1.3 12.5 14.0 15.5 13.0 6.5 1.3 17.0 18.0 20.5 17.0 8.5 1.8 19.5 17.5 21.0 17.5 8.8 2.5 23.0 18.5 27.0 20.5 8.8 2.8 42.0 40.0 52.0 41.0 18 5 5.0 15.5 15.5 19.5 16.5 7.6 1.4 16.0 22.5 26.0 20.5 8.0 2.2 39.0 34.0 49.0 39.0 15.9 4.1 20.5 20.5 24.5 19.5 9.7 2.5 20.0 22.0 24.0 20.0 10.0 2.8 19.0 16.0 21.5 17.5 8.3 1.9 46.0 44.0 53.0 43.5 21.8 5.2 21.0 19.0 22.0 20.0 10.0 2.4 25.0 30.0 33.5 26.5 12.7 3.3 25.5 25.0 31.0 28.0 13 4 1.4 29.5 28.0 35.0 26.0 12.6 4.4 21.0 23.0 28.0 20.5 9.2 3.4 18.5 14.0 20.0 15.5 7.2 2.1 31.0 27.0 41.0 31.5 11.6 3.5 19.0 21.0 26.0 22.0 9.5 1.7 24.0 26.0 27.0 23.5 11.8 3.8 26.0 25.5 30.5 24.0 12.0 3.3 24.0 22.0 28.0 23.0 11.1 2.4 31.0 33.0 33.0 27.0 13.5 6.8 24.0 24.0 30.0 23.5 10.9 3.0 26.0 24.0 30.0 28.5 14.1 0.7 20.0 14.0 21.0 18.0 8.2 1.4 20.5 21.5 23.5 18.0 9.0 2.8 27.0 32.0 37.5 28.0 12.5 4.2 30.5 30.0 36.0 30.0 15.0 3.0 30.0 43.5 48.0 39.0 16.1 3.7 21.0 23.0 25.0 19.0 9.5 3.9 23.0 21.5 27.5 23.0 10.8 2.1 14.0 12.0 16.5 12.0 5.4 2.0 15.5 15.5 17.5 15.0 7.5 1.3 22.0 16.0 24.0 19.5 8.6 2.0 209 Table 67 (cont'd). crystal zone A B C E size width 16.5 15.0 18.5 16.0 8.0 1.3 17.0 15.5 19.0 15.0 7.5 2.0 18.0 19.5 23.0 19.0 9.1 1.9 38.0 28.0 46.0 38.5 14.4 2.8 25.5 21.0 33.0 26.0 9.5 2.6 16.0 21.0 23.5 17.5 7.7 2.6 23.0 21.0 26.5 23.0 11.3 1.7 34.0 30.0 41.5 32.5 14.1 3.9 19.5 18.0 21.5 17.0 8.5 2.3 20.5 23.0 26.5 21.5 10.3 2.4 39.5 39.5 48.5 41.0 19.6 3.6 29.0 16.0 29.5 26.5 10.2 1.2 40.0 30.5 43.0 35.0 16.5 3.8 24.0 18.0 27.0 21.5 9.3 2.4 20.5 20.0 23.0 20.0 10.0 1.5 19.0 18.0 20.5 16.5 8.3 2.0 16.0 16.0 18.0 16.0 8.0 1.0 210 Table 68. Sample Sal How-1 Measurements crystal zone .A B C E size width 33.0 36.0 44.5 36.5 16.0 3.5 15.0 14.5 18.0 13.0 6.3 2.4 10.5 15.5 17.5 14.0 5.5 1.4 20.5 23.0 28.5 22.0 9.4 2.8 20.0 18.5 22.0 17.5 8.8 2.3 21.0 20.0 25.5 19.5 9.1 2.8 19.5 11.0 19.5 14.0 5.6 2.2 15.5 15.5 18.0 13.5 6.8 2.3 17.5 21.0 26.0 20.5 8.2 2.2 12.0 14.5 17.5 14.5 6.1 1.3 15.5 15.0 22.5 19.5 6.6 1.0 16.5 11.5 18.5 16.0 6.5 1.0 24.5 24.5 26.5 24.0 12.0 1.3 17.5 16.5 21.0 15.5 7.3 2.6 25.5 25.5 28.0 23.5 11.8 2.3 23.5 25.0 27.0 25.0 12.5 1.0 18.5 18.0 23.0 21.0 9.6 0.9 50.0 41.0 61.5 51.5 20.6 4.0 31.0 31.0 39.5 31.0 13.9 3.8 33.5 38.5 46.0 42.0 18.7 1.8 15.5 15.5 18.0 14.5 7.3 1.8 30.5 34.0 39.0 33.5 16.3 2.7 14.5 16.5 18.0 15.5 7.8 1.6 37.0 35.5 42.0 36.5 18.3 2.8 14.0 15.0 15.0 12.5 6.3 1.3 34.0 40.0 51.0 40.5 15.7 4.1 34.0 30.0 38.5 30.5 15.0 3.9 27.5 28.5 38.5 30.5 12.0 3.1 24.0 22.0 26.5 22.5 11.3 2.7 36.0 25.5 40.0 32.5 13.6 3.1 19.0 17.0 21.5 19.0 9.5 1.2 18.5 18.5 21.5 19.0 9.5 1.3 34.5 33.0 40.0 31.0 15.5 4.5 211 Table 69. Sample Sal How-6 Measurements crystal zone A B C E size width 33.0 35.0 42.0 35.0 16.5 3.3 12.0 10.5 14.0 10.0 4.6 1.9 33.0 31.0 36.0 32.0 16.0 3.6 19.5 27.0 31.0 23.5 9.5 3.0 16.0 18.5 21.0 18.0 8.7 1.4 14.5 13.5 16.0 15.0 7.5 0.5 30.5 30.5 38.0 34.5 16.1 1.6 26.5 25.0 30.0 26.0 13.0 2.0 17.0 17.5 20.5 16.0 8.0 2.3 15.0 16.0 20.0 17.0 7.5 1.3 16.5 15.0 18.5 17.5 8.8 0.5 25.5 24.5 31.0 27.0 12.7 1.9 28.0 30.5 35.5 32.5 15.8 1.5 20.5 20.0 20.5 18.5 9.3 1.0 30.5 25.0 34.0 28.0 13.2 2.8 31.0 25.0 34.0 28.0 13.4 2.9 12.5 13.0 15.0 11.0 5.5 2.0 26.0 24.0 32.5 22.5 9.7 4.3 46.0 35.5 49.5 40.5 19.2 4.3 12.5 12.0 13.5 10.5 5.3 1.5 24.5 24.5 27.0 21.0 10.5 3.0 32.0 30.0 38.0 29.5 14.1 4.1 22.5 22.0 26.0 21.5 10.8 2.3 22.0 20.5 23.5 19.0 9.5 2.3 38.0 40.0 46.0 36.0 18.0 5.4 46.0 49.0 63.5 55.0 22.7 3.5 27.0 27.0 37.0 30.0 11.8 2.8 18.0 18.5 19.0 17.0 8.5 1.0 26.0 28.0 31.0 29.0 14.5 1.9 21.0 19.5 24.0 21.5 10.8 1.3 212 Table 70. Sample Sal 7-8 Measurements crystal zone A B C E size width 44.6 35.5 51.5 41.5 18.1 4.4 15.5 13.0 18.5 16.5 7.1 0.9 35.0 27.5 39.0 30.5 13.9 3.9 34.0 32.0 38.0 26.5 13.3 6.8 27.0 26.0 30.5 24.0 12.0 3.3 30.5 29.5 44.5 32.0 10.7 4.2 20.5 31.0 32.5 26.5 11.4 2.6 15.5 13.5 18.5 14.5 6.5 1.8 26.0 28.0 34.5 27.5 12.3 3.1 26.0 29.0 34.0 28.0 13.2 2.8 26.5 29.0 34.5 27.0 12.6 3.5 34.0 28.0 39.0 31.0 14.1 3.6 21.5 20.0 26.5 21.0 9.4 2.5 30.5 31.0 37.0 27.5 13.6 4.7 33.0 44.0 47.0 42.5 19.9 2.1 40.0 42.0 46.0 37.5 18.8 6.4 33.5 47.0 54.0 44.5 17.7 3.8 21.5 22.5 26.0 21.0 10.5 2.5 14.0 20.5 22.0 17.0 7.3 2.1 26.5 26.0 32.0 27.0 13.0 2.4 24.5 17.5 29.5 23.0 8.4 2.4 20.5 19.0 22.5 19.5 9.8 1.5 15.0 16.0 19.0 15.5 7.4 1.7 25.0 25.5 29.0 25.5 12.8 1.8 23.0 21.0 25.0 22.5 11.3 2.2 28.0 22.5 33.0 26.5 11.2 2.8 26.5 28.0 36.0 25.0 10.5 4.6 45.5 41.5 52.0 47.0 23.3 2.5 25.0 24.0 29.5 25.0 12.3 2.2 20.5 18.5 23.0 17.5 8.8 2.9 213 Table 71. Sample List for Burlington-Keokuk Formation Hwy 61 Outcrops Sample Number Sample Number of ID Crystals 1 DFS—1 34 2 CAR-5 30 3 MIN—6 34 4 LAK-lO 31 5 MIN—16 33 6 DFS-15 32 7 DFS-24 30 8 LAK—22 30 9 MIN—29 3O 10 LAK-31 30 11 DFS-32 30 12 LAK-36 31 13 DFS—37 30 14 LAK-40 30 15 DUNC-56 30 214 Table 72. Sample DFS-1 Measurements 215 N \l 31. I-' (A) Table 73. Sample CAR-5 Measurements crystal zone A C size width 17.0 .5 20.5 .0 7.7 1.1 30.0 .0 35.0 .0 15.5 2.0 13.0 .0 22.5 .0 6.5 1.6 9.5 .0 11.5 .0 5.0 0.8 .0 .0 32.0 .0 11.4 2.6 .0 .5 23.0 .5 7.9 3.1 .0 .0 12.0 .0 5.0 1.8 .0 .5 16.0 .0 7.0 1.0 .5 .5 23.5 .5 9.3 2.5 .0 .0 24.0 .0 9.9 2.0 .5 .0 27.5 .0 10.1 1.5 .5 .5 14.5 .5 5.3 0.8 .0 5 25.0 .5 11.0 1.2 .0 .5 34.0 .0 14.5 2.5 .0 0 27.0 .5 11.3 2.3 .0 .0 23.0 .0 10.0 2.1 .5 .0 20.5 .0 9.0 1.3 .0 .5 14.5 .0 5.0 2.3 .5 .0 37.0 .5 13.0 4.5 .0 .0 19.5 .0 6.8 2.0 .0 .0 28.0 10.8 3.7 .0 .0 12.0 5.0 1.0 .0 .0 17.5 7.1 1.5 .0 .5 22.0 7.9 2.9 .0 .5 13.5 4.7 2.0 .0 .5 20.5 8.0 2.3 .0 .0 22.5 8.2 2.6 18.0 .5 23.0 7.7 1.9 9.0 .5 13.0 4.2 1.6 .0 .0 O .8 1.8 216 Table 74. Sample MIN-6 Measurements crystal zone A B C E size width 22.0 21.5 26.0 21.5 10.7 2.2 20.0 18.5 22.0 17.0 8.5 2.5 29.0 29.0 34.0 25.5 12.8 4.3 12.0 12.5 14.5 11.5 5.8 1.5 22.0 22.0 26.0 22.5 11.3 1.8 11.5 10.0 18.5 10.0 2.2 1.9 19.0 17.5 20.0 17.5 8.8 1.3 13.5 12.0 16.5 11.0 4.8 2.4 15.5 16.0 22.0 19.0 7.2 1.1 10.0 11.5 12.5 11.5 5.8 0.5 21.0 20.5 22.5 19.5 9.8 1.5 14.0 14.5 17.0 15.5 7.7 0.7 33.0 33.5 35.5 25.0 12.5 5.3 23.0 16.5 25.0 18.0 7.9 3.1 12.5 12.0 14.5 12.5 6.3 1.0 13.0 12.0 14.0 12.5 6.3 0.8 15.5 11.0 16.5 14.5 6.5 0.9 9.5 8.5 10.0 8.0 4.0 1.0 44.0 32.0 53.0 41.5 15.4 4.3 19.5 25.5 27.5 24.0 11.3 1.6 23.0 23.0 25.0 19.0 9.5 3.0 28.0 28.0 29.0 22.0 11.0 3.5 19.5 17.5 22.5 16.5 8.0 2.9 11.0 9.0 11.0 9.0 4.5 1.6 43.0 42.0 53.0 41.0 19.1 5.6 15.0 16.5 19.5 17.5 8.2 0.9 13.0 19.0 21.0 16.0 6.5 2.0 18.5 20.0 19.5 17.5 8.8 1.0 16.5 15.0 19.5 17.5 8.2 0.9 23.5 22.5 25.0 19.0 9.5 3.0 14.5 15.5 19.0 12.5 5.7 2.9 16.5 18.0 20.0 15.0 7.5 2.5 27.0 28.0 31.0 29.0 14.5 1.0 24.0 24.0 33.0 24.5 9.6 3.3 217 Table 75. Sample LAK-lO Measurements crystal zone A B C E size width 28.0 26.5 28.0 10.0 5.0 9.0 16.5 14.5 17.0 14.0 7.0 2.6 40.5 39.0 50.0 35.0 16.1 6.9 20.0 20.0 25.0 18.0 8.3 3.2 18.0 21.5 26.0 22.5 9.5 1.5 19.5 19.5 23.0 19.0 9.5 2.0 19.5 20.0 20.0 16.0 8.0 2.0 21.0 18.5 25.0 19.0 8.6 2.7 15.0 13.5 14.5 10.5 5.3 2.0 14.5 15.0 17.5 14.0 7.0 1.8 12.5 12.5 13.5 12.0 6.0 0.8 29.0 20.5 30.5 24.0 10.9 3.0 21.5 28.5 35.5 28.0 10.1 2.7 22.0 22.0 25.0 20.0 10.0 2.5 16.0 17.0 18.0 16.0 8.0 1.0 18.5 20.0 25.0 19.0 8.2 2.6 31.5 30.0 34.0 28.0 14.0 3.0 15.5 16.5 19.0 16.0 8.0 1.5 35.5 30.0 42.0 33.0 14.5 4.0 11.5 11.5 13.0 10.0 5.0 1.5 31.0 33.0 35.0 27.5 13.8 6.1 26.5 30.0 34.0 28.0 13.7 2.9 13.0 15.0 15.5 11.5 5.8 2.8 22.5 22.0 27.0 20.0 9.7 3.4 24.0 25.5 31.0 27.0 12 5 1.8 10.5 11.0 13.0 11.5 5.6 0.7 19.0 20.0 23.0 20.5 10. 1.3 27.0 29.0 31.0 25.0 12.5 4.8 13.0 13.0 16.0 13.0 6.2 1.4 25.0 23.5 26.5 19.5 9.8 3.5 218 Table 76. Sample MIN-16 Measurements crystal zone A B C E size width 21.5 32.5 35.0 30.0 12.4 2.1 38.0 38.5 45.0 37.0 18.5 4.0 14.0 12.5 14.0 11.5 5.8 1.3 19.0 23.0 28.0 22.0 9.0 2.5 12.0 13.5 13.5 12.0 6.0 0.8 22.0 24.0 28.0 15.5 7.5 6.0 26.0 22.0 29.0 23.0 11.2 2.9 24.5 23.0 27.5 20.5 10.3 3.5 12.5 13.0 15.5 12.5 6.1 1.5 18.5 17.5 21.0 18.0 9.0 1.5 13.0 11.0 15.0 10.0 4.6 2.3 12.0 12.0 14.0 11.0 5.5 1.5 20.5 13.0 22.0 16.5 6.6 2.2 27.5 27.0 29.0 26.0 13.0 1.5 8.5 9.5 11.0 9.0 4.3 1.0 14.5 16.0 18.0 16.0 8.0 1.0 14.5 15.0 17.0 15.0 7.5 1.0 13.5 15.0 16.0 14.5 7.3 0.8 15.5 16.0 18.5 15.0 7.5 1.8 15.0 12.0 17.0 14.0 6.3 1.4 12.5 13.5 15.0 12.0 6.0 1.5 23.0 22.0 24.5 20.5 10.3 2.0 16.5 12.0 20.0 13.5 5.0 2.4 15.0 17.0 21.0 15.5 6.6 2.3 23.5 24.0 26.0 20.0 10.0 3.0 15.5 15.0 18.5 14.0 6.8 2.2 22.0 24.0 25.0 20.0 10.0 4.3 17.5 18.5 20.0 14.5 7.3 2.8 13.0 12.0 13.5 12.0 6.0 0.8 20.0 22.0 26.0 21.0 9.9 2.3 11.0 10.0 13.0 8.5 4.0 2.1 19.5 17.5 23.0 20.0 9.3 1.4 14.5 17.0 19.0 18.0 8.8 0.5 219 Table 77. Sample DFS-15 Measurements crystal zone .A B C E size width 30.0 29.0 36.0 33.0 15.9 1.4 30.5 29.0 35.5 33.0 16.5 1.2 13.0 14.0 15.0 11.0 5.5 2.0 17.0 18.5 22.0 14.0 6.6 3.8 14.0 16.0 18.0 13.0 6.4 2.5 21.5 29.0 34.0 29.0 11.5 2.0 24.5 17.0 26.5 21.0 9.0 2.4 23.0 14.0 24.5 18.5 7.2 2.3 16.0 15.0 19.0 13.5 6.5 2.6 11.0 11.0 14.0 12.0 5.4 0.9 31.5 34.0 40.5 31.0 14.6 4.5 21.5 22.5 26.0 19.5 9.8 3.3 14.0 18.5 20.0 18.0 8.3 0.9 24.5: 25.0 27.5 24.0 12.0 1.8 11.0 11.5 11.5 10.0 5.0 0.8 17.5 16.0 18.0 14.0 7.0 2.0 17.0 17.0 21.5 17.0 7.7 2.0 12.0 11.5 14.0 10.5 5.3 1.8 15.5 17.5 18.5 15.5 7.8 2.3 15.0 13.0 15.0 12.0 6.0 2.7 17.5 17.5 20.0 17.5 8.8 1.3 16.0 18.0 18.5 16.0 8.0 2.5 32.0 31.5 41.5 35.5 15.3 2.6 11.5 11.5 12.0 11.0 5.5 0.5 12.5 14.0 14.5 11.0 5.5 1.8 32.0 30.5 38.0 30.0 14.5 3.9 37.0 32.0 42.0 32.5 15.6 4.6 24.0 16.0 25.0 18.5 8.1 2.9 19.0 20.0 20.0 16.0 8.0 2.0 14.5 13.0 17.5 13.5 6.1 1.8 32.0 29.0 37.0 30.5 14.8 3.2 17.0 15.0 18.0 15.5 7.8 2.0 220 Table 78. Sample DFS—24 Measurements crystal zone A B C E size width 20.0 22.0 24.0 17.0 8.5 4.3 19.0 18.0 20.0 16.5 8.3 1.8 27.5 19.0 29.0 22.0 9.8 3.1 17.0 16.5 19.5 16.0 8.0 1.8 16.0 14.0 17.0 14.0 7.0 2.1 23.0 24.5 28.0 16.0 8.0 6.0 19.0 18.0 21.0 18.0 9.0 1.5 20.0 16.0 22.0 18.0 8.5 1.9 23.0 20.0 26.0 20.5 10.0 2.7 30.0 22.0 32.0 26.5 12.2 2.5 13.0 14.5 16.0 12.5 6.3 1.8 18.0 20.0 20.0 18.0 9.0 2.9 10.0 11.0 12.0 9.5 4.8 1.3 23.0 25.5 30.5 24.5 11.2 2.7 15.0 15.0 17.0 13.5 6.8 1.8 22.0 23.0 24.0 19.5 9.8 2.3 14.5 14.0 18.0 14.0 6.4 1.8 28.0 29.0 36.0 27.5 12.5 3.9 23.0 23.5 23.0 16.0 8.0 3.5 19.0 15.5 21.0 17.0 8.1 1.9 18.0 16.5 20.0 17.0 8.5 1.5 20.0 21.0 26.0 21.0 9.5 2.3 15.0 14.0 16.0 10.0 5.0 3.0 14.0 14.0 15.0 11.5 5.8 1.8 18.0 13.5 20.0 15.0 6.6 2.2 18.5 19.0 24.0 19.0 8.5 2.2 56.0 48.0 72.0 57.0 21.9 5.8 9.0 10.0 13.0 10.0 3.9 1.2 56.0 47.0 69.0 56.0 22.8 5.3 22.5 21.0 25.0 19.0 9.5 3.0 221 Table 79. Sample LAK—22 Measurements crystal zone A B C E size width 22.5 24.5 29.0 24.0 11.3 2.4 21.0 18.5 24.0 17.5 8.4 3.1 19.0 17.5 21.0 19.0 9.5 1.0 14.5 10.0 16.0 14.5 6.0 0.6 26.0 24.0 33.0 25.5 10.8 3.2 28.0 23.0 31.0 23.5 11.3 3.6 27.5 36.0 39.0 35.0 16.3 1.9 36.0 35.0 42.0 37.0 18.5 2.5 17.0 15.0 18.0 15.0 7.5 2.3 20.5 18.5 24.0 20.0 9.5 1.9 17.5 19.0 20.0 15.5 7.8 2.3 22.0 23.0 25.5 22.0 11.0 1.8 24.5 20.0 29.0 23.0 9.8 2.6 27.5 27.0 31.5 24.0 12.0 3.8 24.0 23.5 28.0 24.0 12.0 2.0 22.5 22.0 27.0 25.5 12.4 0.7 20.5 19.0 23.0 20.5 10.3 1.3 14.5 14.0 15.0 13.5 6.8 0.8 18.0 18.0 21.5 19.5 9.7 1.0 18.0 19.0 21.0 18.0 9.0 1.5 16.0 14.0 16.0 12.0 6.0 3.3 18.5 17.5 23.0 21.0 9.4 0.9 14.5 14.0 17.0 15.5 7.7 0.7 31.0 28.5 36.0 28.0 13 6 3.9 23.5 24.0 29.0 23.0 11.1 2.9 14.5 16.0 19.0 15.5 7.2 1.6 27.5 29.0 31.0 28.0 14.0 1.5 31.5 33.0 38.0 30.0 15.0 4.0 26.5 23.5 30.0 23.5 11.6 3.2 10.5 11.0 14.0 11.5 5.0 1.1 Table 80. Sample MIN-29 Measurements crystal zone A. B C E size width 12.5 13.0 15.0 13.0 6.5 1.0 19.0 16.0 22.0 16.0 7.3 2.7 17.0 16.5 18.5 13.5 6.8 2.5 13.0 14.0 17.5 14.0 6.1 1.5 27.5 27.0 31.0 22.0 11.0 4.5 13.0 14.0 16.0 10.5 5.3 2.8 14.0 13.5 16.0 14.0 7.0 1.0 29.5 31.0 34.0 28.5 14.3 2.8 19.0 17.0 20.5 15.5 7.8 3.2 15.5 15.0 17.0 13.5 6.8 1.8 13.0 13.0 17.5 12.0 4.9 2.2 20.0 18.5 23.0 17.0 8.5 3.0 16.0 15.5 17.0 13.5 6.8 1.8 20.5 21.5 28.5 22.5 9.0 2.4 14.5 14.5 16.0 12.0 6.0 2.0 17.5 19.0 21.0 18.0 9.0 1.5 16.0 20.0 24.0 20.0 8.2 1.6 12.0 12.0 13.5 12.0 6.0 0.8 14.0 13.5 16.0 15.0 7.5 0.5 12.0 10.0 11.5 8.0 4.0 2.9 15.5 16.0 17.5 14.5 7.3 1.5 15.5 15.5 20.0 16.0 7.0 1.8 33.5 26.5 37.5 32.5 14.8 2.3 19.5 15.5 24.0 19.0 7.4 1.9 23.5 25.0 32.0 28.0 11.8 1.7 21.5 21.5 27.0 22.5 10.4 2.1 18.0 17.0 18.0 13.5 6.8 2.3 21.0 19.0 23.0 18.0 9.0 3.1 13.5 11.0 15.0 13.0 6.1 0.9 20.0 20.0 27.5 21.5 8.4 2.4 223 Table 81. Sample LAK-31 Measurements crystal zone A B C E size width 14.0 14.5 18.0 16.5 7.5 0.7 36.0 32.5 42.0 36.0 17.2 2.9 36.0 34.0 42.0 36.5 18.1 2.7 28.5 30.0 36.0 30.5 14.5 2.6 20.5 22.0 25.0 20.0 10.0 2.5 28.0 28.0 33.0 24.5 12.3 4.3 24.0 23.5 27.0 23.5 11.8 1.8 28.0 28.0 31.5 27.5 13.8 2.0 19.5 18.0 20.0 13.0 6.5 3.5 9.0 9.5 12.0 9.5 4.1 1.1 29.5 32.5 37.5 31.5 15.4 2.9 19.5 23.0 28.0 20.5 8.6 3.2 21.0 20.5 24.0 20.5 10.3 1.8 26.0 25.0 30.0 25.5 12.8 2.3 30.0 32.0 37.0 30.0 15.0 3.4 16.0 16.0 18.5 15.5 7.8 1.5 15.5 18.0 21.0 16.0 7.3 2.3 23.0 26.0 30.0 26.0 12.4 1.9 28.0 30.0 34.0 26.5 13.3 4.2 27.0 27.0 31.0 23.5 11.8 3.8 22.0 26.5 33.0 30.0 11.9 1.2 50.0 36.5 62.5 49.0 17.0 4.7 23.0 26.0 34.5 30.5 11.4 1.5 28.0 22.5 36.0 27.0 9.7 3.2 23.5 25.5 26.0 21.5 10.8 4.6 29.5 27.5 31.0 22.5 11.3 6.5 20.5 21.0 26.0 23.0 10.6 1.4 20.5 26.0 30.0 27.0 11.7 1.3 13.0 13.0 16.0 13.0 6.2 1.4 36.0 36.5 46.0 33.0 14.9 5.9 224 Table 82. Sample DFS-32 Measurements crystal zone .A B C E size width 15.0 13.5 18.0 15.0 6.8 1.4 19.5 18.0 21.5 17.0 8.5 2.3 16.0 15.0 17.0 15.0 7.5 1.0 24.5 23.5 29.0 25.0 12.2 2.0 10.0 10.0 13.0 11.5 5.0 0.7 17.5 16.0 18.0 9.5 4.8 4.3 15.0 16.5 18.0 15.5 7.8 1.3 15.5 15.0 18.0 14.5 7.3 1.8 16.5 18.5 22.0 17.5 8.0 2.1 19.0 17.0 21.0 16.0 8.0 2.8 16.5 14.0 19.0 14.5 6.7 2.1 26.0 24.0 28.5 20.5 10.3 5.0 19.0 19.0 20.0 16.5 8.3 1.8 27.0 25.5 33.5 30.0 13.4 1.6 15.0 11.0 17.0 14.0 5.8 1.3 15.5 15.5 18.0 13.5 6.8 2.3 15.0 17.0 17.0 14.0 7.0 3.0 11.5 13.0 14.5 11.0 5.5 1.8 17.0 19.0 21.0 15.5 7.8 3.1 20.0 20.0 24.0 20.5 10.1 1.7 20.5 22.0 25.0 22.0 11.0 1.5 16.0 18.0 20.0 17.0 8.5 1.7 20.5 22.5 27.0 22.5 10.3 2.1 17.0 19.0 25.0 22.0 8.4 1.2 37.0 36.0 44.0 37.0 18.2 3.4 20.5 18.5 19.5 15.5 7.8 4.7 19.5 18.5 21.0 17.5 8.8 1.8 27.0 29.0 28.0 25.5 12.8 5.2 12.5 12.0 14.0 10.5 5.3 1.8 18.5 17.5 23.0 20.0 8.9 1.3 225 Table 83. Sample LAK-36 Measurements crystal zone A. B C E size width 13.5 12.5 14.0 13.0 6.5 0.5 12.0 14.5 16.0 13.0 6.3 1.5 31.0 29.0 33.0 25.5 12.8 5.8 15.0 14.0 17.0 15.0 7.5 1.0 38.5 38.0 44.0 33.0 16.5 5.5 14.0 13.5 14.0 10.0 5.0 2.0 11.0 10.0 12.0 9.0 4.5 1.5 19.5 17.0 22.0 18.0 8.8 2.0 14.5 15.5 17.5 13.5 6.8 2.0 13.5 21.5 22.0 17.0 7.3 2.1 18.5 18.0 20.0 17.5 8.8 1.3 31.0 33.0 40.0 32.5 15.1 3.5 24.0 25.0 32.5 22.5 9.4 4.2 12.5 14.0 14.5 13.5 6.8 0.5 16.5 16.0 19.0 17.0 8.5 1.0 22.0 20.0 27.0 21.0 9.3 2.6 19.0 18.0 21.0 16.0 8.0 2.5 22.0 15.5 23.0 18.0 8.3 2.3 37.0 39.0 42.0 33.0 16.5 7.0 23.5 24.0 26.0 19.0 9.5 3.5 18.5 18.0 22.5 17.0 8.1 2.6 20.5 20.0 22.0 18.5 9.3 1.8 23.5 22.5 28.0 21.0 10.2 3.4 19.0 22.0 26.0 20.0 9.0 2.7 16.5 12.0 17.5 16.0 7.4 0.7 12.5 12.5 14.5 11.5 5.8 1.5 19.0 19.0 24.0 18.5 8.4 2.5 20.0 19.0 26.0 19.5 8.1 2.7 28.0 24.0 34.0 22.0 9.4 5.1 22.0 23.5 26.0 23.0 11.5 1.5 24.5 28.0 32.0 25.0 12.0 3.4 226 ' 4‘.-!'2U*..~ev entrant-1:4 out-2‘ Table 84. Sample DFS-37 Measurements crystal zone A. B C E size width 26.0 25.5 31.0 27.0 13.3 2.0 21.5 20.0 24.0 18.5 9.3 2.8 28.5 26.5 32.0 27.0 13.5 3.1 32.0 34.0 38.0 32.5 16.3 3.8 20.5 21.0 24.5 17.0 8.5 3.8 17.5 16.0 21.0 18.0 8.3 1.4 26.0 19.0 28.0 24.0 10.9 1.8 18.0 16.0 19.5 16.5 8.3 2.0 26.0 27.0 33.0 25.5 11.9 3.5 27.0 25.0 29.0 23.0 11.5 4.5 36.0 38.0 44.0 32.0 16.0 6.1 32.0 30.0 36.0 28.5 14.3 4.5 27.5 29.0 33.0 26.5 13.3 3.3 20.0 18.0 23.0 17.5 8.5 2.7 31.5 30.0 37.0 27.5 13.5 4.7 21.0 22.0 23.5 16.5 8.3 3.5 26.5 28.0 30.0 26.0 13.0 2.0 26.0 23.5 30.0 24.0 11.7 2.9 20.0 22.0 22.0 18.5 9.3 4.0 29.0 27.0 32.0 26.5 13.3 3.8 25.0 23.0 27.5 23.0 11.5 3.1 20.0 20.0 23.0 16.5 8.3 3.3 34.5 32.5 39.5 33.0 16.5 3.6 25.0 27.0 29.5 24.5 12.3 3.6 24.5 26.5 29.5 24.0 12.0 3.4 19.5 20.0 22.5 18.5 9.3 2.0 17.0 15.0 17.0 12.0 6.0 4.0 34.5 34.0 41.0 32.0 15.9 4.5 15.0 13.5 17.0 15.0 7.5 1.0 37.0 35.0 36.5 27.0 13.5 9.5 227 q Table 85. Sample LAK-40 Measurements crystal zone .A B C E size width 20.0 19.5 22.0 17.5 8.8 2.3 32.0 34.0 41.0 27.5 12.9 6.3 22.5 25.0 28.5 24.5 12.1 2.0 25.5 27.0 27.0 22.0 11.0 2.5 27.0 29.0 33.5 28.5 14.2 2.5 39.0 45.0 51.0 43.5 21.0 3.6 30.0 28.0 35.5 29.0 13.9 3.1 17.0 17.0 20.0 16.5 8.3 1.8 39.0 34.0 44.0 38.0 18.6 2.9 18.5 18.5 20.5 16.0 8.0 2.3 25.0 27.0 29.0 25.0 12.5 3.5 24.0 30.0 34.0 25.0 11.3 4.1 27.5 29.0 32.0 26.5 13.3 2.8 27.0 27.0 32.0 27.0 13.5 2.5 26.5 32.5 38.0 29.5 12.8 3.7 19.5 19.5 22.0 19.0 9.5 1.5 19.0 17.0 21.0 18.0 9.0 1.8 25.5 29.0 37.0 30.5 12.2 2.6 27.0 30.0 36.0 32.5 14.8 1.6 28.0 28.5 28.0 24.5 12.3 1.8 32.0 31.0 39.0 33.0 15.5 2.8 35.0 28.0 39.0 30.0 13.9 4.2 14.0 15.5 18.0 15.0 7.2 1.4 40.0 35.5 47.0 36.0 16.7 5.1 21.0 19.0 24.0 17.0 8.4 3.5 17.0 16.5 19.0 14.5 7.3 2.3 30.0 28.5 29.0 26.0 13.0 1.5 19.0 18.0 22.0 18.5 9.3 1.8 20.0 20.0 21.0 16.0 8.0 2.5 18.0 17.0 14.0 13.5 6.8 0.3 228 Table 86. Sample DUNC—56 Measurements crystal zone .A B C E size width 18.0 14.5 20.5 14.0 6.3 2.9 16.0 18.0 17.5 15.5 7.8 3.0 25.0 23.0 24.0 21.0 10.5 4.9 17.0 20.0 24.0 20.0 8.6 1.7 17.0 17.0 22.0 19.0 8.3 1.3 27.0 26.0 36.0 30.0 12.0 2.4 36.0 35.0 44.0 41.0 19.3 1.4 42.0 43.0 46.0 40.5 20.3 2.8 25.0 23.5 29.5 24.0 11.6 2.7 18.0 18.5 24.0 19.0 8.1 2.1 27.0 27.0 32.0 26.0 13.0 3.0 33.5 28.0 37.0 31.0 15.1 2.9 15.5 14.0 17.5 14.5 7.3 1.5 10.5 11.0 15.0 12.0 4.6 1.1 22.0 19.0 25.0 23.0 11.0 1.0 19.0 18.0 19.5 15.0 7.5 2.3 25.0 23.5 28.0 26.0 13.0 1.0 30.0 31.0 41.0 37.0 15.1 1.6 17.0 21.0 23.5 19.0 8.8 2.1 42.0 46.0 57.0 46.0 20.0 4.8 23.0 21.0 24.5 21.5 10.8 2.8 29.5 29.0 36.0 30.0 14.3 2.9 15.5 14.5 18.5 14.5 6.9 1.9 15.5 17.5 18.0 14.0 7.0 3.2 14.5 16.0 18.0 14.5 7.3 1.8 19.5 23.0 26.0 23.0 10.9 1.4 17.0 19.0 22.0 15.5 7.4 3.1 26.0 26.5 29.0 24.5 12.3 2.3 16.0 18.0 21.0 16.0 7.5 2.4 24.0 22.5 28.0 24.0 11.8 2.0 229 7"Plvt"’.‘f':9".'7FCIIE\§‘tI rf.‘::'9\§(t_¢‘ .‘- 5791511593541“:inn-.4 '1'." Table 87. Sample List for Seroe Domi Formation, Seru Blandan and St. Michielsburg Outcrops Sample Number Sample Number of ID Crystals 1 SB-l Zone I 30 2 SB-2 Zone I 20 3 SM-l Zone I 15 4 SB-l Zone II 30 5 SB—2 Zone II 20 6 SM-l Zone II 15 230 Table 88. ..x-s 16.-"-(-:9'.-_r_~(5rg. 0‘ ._. t!:(~\v"" .4 f " Sample SB-l Zone I Measurements crystal zone .A B C E size width 38.5 38.0 45.0 35.0 17.5 5.0 37.5 35.5 41.0 34.0 17.0 5.4 29.5 29.5 36.5 25.5 12.0 5.2 41.0 41.5 47.0 36.5 18.3 5.3 45.5 44.0 59.0 46.5 19.7 5.3 40.0 38.0 40.5 36.0 18.0 6.7 27.0 26.0 31.0 26.0 13.0 2.5 33.5 30.0 38.0 31.5 15.6 3.2 40.0 40.5 45.5 38.5 19.3 3.5 21.5 25.0 29.0 25.0 11.6 1.8 24.0 27.0 31.0 25.5 12.3 2.7 33.0 23.0 35.0 28.5 12.7 2.9 27.5 29.0 34.0 28.5 14.0 2.7 46.0 33.0 51.0 46.0 19.5 2.1 44.0 42.0 46.0 42.0 21.0 6.0 28.0 30.0 36.0 28.0 13.1 3.7 39.0 37.0 45.0 41.0 20.5 2.2 29.0 26.0 33.0 27.0 13.3 3.0 40.0 37.0 48.0 38.0 17.7 4.6 36.0 34.0 41.0 36.0 18.0 3.0 36.5 35.0 10.0 34.0 17.0 3.0 37.0 29.0 41.0 35.0 16.1 2.8 34.0 32.0 39.0 34.0 17.0 2.7 38.0 36.0 39.0 35.0 17.5 5.8 50.0 52.0 57.5 49.0 24.5 6.8 42.5 44.0 48.0 39.0 19.5 4.5 28.0 30.0 33.0 29.0 14.5 3.2 49.0 48.0 52.0 46.0 23.0 3.0 32.0 32.5 39.0 35.0 17.1 2.0 43.0 41.0 47.0 41.0 20.5 5.3 231 Table 89. Sample SB-l Zone II Measurements zone A B E width 30.5 28.0 4.0 2.0 15.4 28.5 28.5 8.5 4.2 12.7 22.0 24.0 3.0 1.5 12.7 32.0 30.0 9.0 4.5 14.1 37.0 37.5 12.5 5.8 15.8 32.0 28.0 7.0 3.4 14.3 21.0 22.5 4.5 2.2 10.7 26.0 23.0 6.5 2.9 11.0 31.0 32.0 8.5 4.1 14.4 18.0 23.0 3.5 1.7 10.2 18.0 23.0 4.0 1.8 9.9 23.0 18.0 2.5 0.9 9.8 22.0 25.0 2.0 1.0 12.8 37.0 32.0 13.0 5.4 13.6 38.0 31.0 11.5 5.5 14.6 24.0 26.0 2.5 1.3 14.1 37.5 30.0 12.5 6.0 13.6 23.0 22.0 5.0 2.5 10.9 30.0 32.0 9.0 4.3 13.9 32.0 27.5 3.0 1.5 16.0 28.0 28.0 7.0 3.4 13.1 30.0 27.0 8.0 3.8 12.8 29.0 28.0 7.0 3.5 13.5 34.0 32.0 9.0 4.5 16.2 37.0 44.0 15.0 7.3 16.4 37.0 38.0 9.0 4.5 15.0 22.0 25.0 6.0 2.8 10.8 39.0 41.0 17.0 8.5 15.8 28.0 28.5 8.0 3.8 12.7 35.0 35.0 11.0 5.5 15.0 Table 90. Sample SB—2 Zone I Measurements crystal zone A B C E size width 45.0 41.0 52.0 44.5 21.7 3.7 17.0 17.0 21.0 17.5 8.3 1.7 10.0 10.0 10.0 9.5 4.8 0.3 40.5 46.0 52.0 43.5 21.4 4.2 11.0 10.5 12.0 9.5 4.8 1.3 19.5 19.5 23.0 20.0 10.0 1.5 40.0 38.0 47.0 42.0 20.6 2.5 26.0 28.0 31.0 26.5 13.3 3.1 33.0 34.0 39.0 34.0 17.0 2.5 39.0 36.0 48.0 41.0 18.2 3.1 54.0 54.0 62.0 55.0 27.5 3.5 42.0 38.0 48.0 40.5 20.0 3.7 30.0 33.0 43.0 35.0 13.9 3.2 31.0 31.0 33.0 29.5 14.8 1.8 31.0 31.0 42.5 35.0 13.8 3.0 19.0 17.0 21.0 17.0 8.5 2.3 24.0 25.5 30.0 26.0 12.7 1.9 22 0 22.5 25.0 21.0 10.5 2.0 26.0 25.0 29.0 23.0 11.5 3.0 31.0 30.0 32.0 26.5 13.3 2.8 233 Sample SB—2 Zone II Measurements Table 91. h masssssomezsemionoggoa o.4..7..211475201..... zml8313711111111166797 a tazc35363838170.325830254 S 0.0.0.0... 0.0.0.0.. ”.86213116244m444213223 C R~055500.500.0.000000500 E .0... o. coco-coo. 3 4 00 15272415912999738458 55555005000505000005 O. . ......OOOOOOCCO C479.39.026415059576136 41 4 242345432312222 00000000005050005500 B16393644816177722820 31 3 132234322212122 00000000000050505000 A288.3&522657586445610 41 3 132234322211122 234 Table 92. Sample SM-l Zone I Measurements crystal zone A B C E size width 48.0 48.0 54.0 48.0 24.0 3.0 48.0 46.0 55.0 46.0 23.0 5.3 42.0 37.0 49.0 43.0 20.1 2.8 44.5 43.0 55.0 50.0 23.0 2.3 49.0 40.0 54.0 46.0 22.1 3.8 49.0 39.0 58.0 46.0 19.2 5.0 69.0 60.0 80.0 73.0 34.1 3.3 59.0 49.0 65.0 57.0 27.8 3.9 45.0 47.0 57.0 48.0 22.6 4.2 55.0 57.0 69.0 62.0 29.4 3.3 37.0 37.0 36.0 32.0 16.0 2.0 36.0 38.0 43.0 36.0 18.0 4.3 34.0 40.0 45.0 38.0 18.3 3.4 51.5 55.0 64.0 52.0 25.6 5.9 28.0 28.0 33.0 29.0 14.5 2.0 235 Table 93. Sample SM—l Zone II Measurements crystal zone .A B C size width 39.0 38.0 48.0 1 5 5.4 17.0 39.0 38.0 46.0 11 0 5.5 17.4 34.0 29.0 43.0 11 0 4.3 12.6 34.0 39.0 50.0 11 0 4.3 15.3 40.0 34.0 46.0 2.1 19.3 40.0 37.0 46.0 3.7 19.2 55.0 55.0 73.0 1 .0 8.0 22.6 50.0 39.0 57.0 1 5 5.9 19.0 35.5 40.0 48.0 2.7 18.9 45.0 49.0 62.0 6.3 19.8 31.0 29.0 32.0 4.5 14.3 26.0 32.0 36.0 4.2 12.5 30.0 33.0 38.0 5.1 13.5 40.0 45.0 52.0 4.3 20.6 22.0 22.0 29.0 3.4 8.9 236 BIBLI OGRAPHY 237 BIBLIOGRAPHY Badiozamani, Khosrow, 1973, The Dorag Dolomitization Mbdel - Application to the Middle Ordovician of Wisconsin, Journal of Sedimentary Petrology, volume 43, p. 965- 984. Baker, Paul A. and Kastner, Miriam, 1981, Constraints on the Formation of Sedimentary Dolomite, Science, volume 213, p. 214—216. Banner, Jay L., Hanson, G. 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