235.

CHAPTER 8

Sut·111ARY

Detailed petrographic, mineralogical, chemical and isotopic studies of the previously poorly documented southern and southeastern portionsof the composi tc Permo-Carboniferous :~ew England Batholi th have delineated a number of distinct igneous suites. The Hillgrove Suite, from which this study arose, has been restricted from its original definition, which included both mafic and felsic rocks, to those plutons which constitute predominantly the south­ eastern flank of the batholitic "core" (Fig. 2.1) and which display features characteristic of S-type granitoids (Chapter 3). This suite is intruded into thick sequences of radiometrically dated predominantly Devonian and Carboniferous volcanogenic greywackes, siltstones and shales. Relatively thin veneers of locally fossiliferous Early Permian sediments unconformably overlie these older sediments. Recognition of these unconformities has been exceedingly difficult because bedding and exposure are generally poor, lithologies are very similar, but more importantly, because the entire sequence, including the younger beds, was strongly deformed during the early­ and mid-Permian.

A sequence of major tectonic events commenced in New England during the early- to mid-Carboniferous which resulted in the generation of voluminous quantities of granitoids and related rocks. The first of these events is considered to have been a downbuckling of the moderately thick sedimentary pile into a PIT environment in which partial melting occurred (- 680- 700°C). The composition of the intermediate to felsic volcanogenic detritus was such that substantial quantities of minimum melt were produced. A temporary cessation of compressive forces allowed the melts to coalesce, then move upwards despite only small density contrasts between the magma and the relatively plastic metasediments. The extent to which these melts moved away from their sites of generation appears to have been related to their degree of water-saturation, the composition of the enclosing metasediments and the distribution of compressive forces. Thus, granitoids of the Hillgrove Suite which display minimal contact metamorphic effects and are associated with major faults, e.g. the Hillgrove, Enmore and Kilburnie Adamellites, rose higher in the crust than those which are surrounded by a mantle of high-grade metamorphics, e.g. the Argyll, Tia and Abroi Granodiorites. 236.

A derivation of the Carboniferous Hillgrove Suite granitoids from the exposed Devonian greywackes and intercalated pelitic rocks is consistent with mineralogical and chemical data, with the time gap (60- 100 m.y.) between sedimentation and granitoid formation noted elsewhere, and with the fact that these possible source rocks had essentially the same 87S r J86Sr ratios at - 320 m.y. as the initial 87Sr /86Sr ratio of the granitoids. However, RE and other selected trace element data preclude a derivation for the Hillgrove Suite by partial melting of the sediments which surround the granitoids at the present erosion level but suggest that similar, though less REE-enriched sediments such as those of the Tamworth Trough, may be an essential component of the source. Comparison of the granitoid and mineral compositions with experimental phase equilibrium studies suggest that the majority of plutons were generated and crystallized between 4 and 7 kb F1120. However, final emplacement (or uplift) may not have occurred for some time, as shown by the consistently younger biotite ages compared with total-rock ages. Variations in some of the biotite ages are concluded to reflect differences in the amount of vertical movement of the granitoids from the zone of magma generation.

The association of the calc-alkaline mafic intrusive complexes with the Hillgrove Suite granitoids appears to be related to the compressive phase which accompanied emplacement of the latter. Sr isotopic ages and field relations suggest that the time period between the emplacement of the granitoids and of the calc-alkaline complexes may have been small (- 10-20 m.y.). Petrographic, mineralogical, chemical and Sr isotopic data suggest that these complexes are products of contaminated tholeiitic basaltic magma.

During the early Permian a second and significantly more-extensive downbuckling of the somewhat thicker New England sedimentary pile occurred, bringing it into close proximity with the upper mantle. The higher temperatures triggered a complex sequence of progressive fractional melting events which yielded felsic granitoids, adamellites, granodiorites, diorites, microtonalites and monzonites. These comprise the New England Suite. The sequence of fractional melting, accumulation of residual ferromagnesian phases, and remelting of the latter, produced an extreme diversity of textural, mineralogical and chemical features, previously interpreted as resulting from partial melting of igneous source rocks or by fractional crystallization of enriched upper mantle material. Sr isotopic data provide convincing evidence to support my 237.

model that the plutons of this Suite are consangineous,having been derived from essentially the same type of sedimentary source material which yielded the plutons of the Hillgrove Suite, although specific areas within this source material may have differed slightly in chemical composition. The Sr isotopic data furthermore provide sound evidence that it is highly unlikely for the source material of either the J:\eH England or Hillgrove Suites to have contained a Precambrian component or that Precambrian continental crust underlies the Ne\"r England Fold Belt.

The downbuckling of the crust during the early Permian to produce the New England Suite, and its subsequent "rebounding", is coincident with major diastrophism over the entire New England Fold Belt. Severe compression along the locus of the Hillgrove Suite especially caused extensive folding and faulting, superposing a well-developed, sometimes bi-directional, tectonite fabric onto an earlier fabric in these granitoids. In addition, the

di~trophism during this period may possibly have caused a further slight uprise of some Hillgrove Suite plutons, so that they became even more effectively isolated from any subsequent periods of lower crustal magma generation and intrusion. This is suggested by the older biotite ages of certain "high-level" plutons compared with those plutons which remained close to their site of generation.

The major crustal fracturing in the area of the Hillgrove Suite, during the period accompanying "rebound" and the emplacement of the relatively deeply generated New England Suite, permitted intrusion of some of the upper mantle material which provided the heat source for the Permian melting events. This upper mantle material, represented by the tholeiitic intrusive complexes associated with the Hillgrove Suite, is manifest at the present level of exposure, as comparatively small igneous complexes. The primitive chemical and isotopic characteristics of the olivine gabbros in these complexes has generally been preserved despite their emplacement through rather thick crust. However, minor contamination of the gabbroic magma by crustal material during the early stages of its ascent, followed by crystal accumulation and intense

fractional crystallization at various conditions of f02 and aH20, produced a wide range of derivatives. The early and middle stages of fractionation are characterized by absolute iron-enrichment; this is expressed mineralogically by the crystallization of ilmenite in the dioritic rocks and by very iron-rich amphiboles and biotites in the granophyres. Although the adamellites and more-felsic rocks follow a trend which is dominated by alkali enrichment, 238. their chemistry and mineralogy reflect a history of fractional crystallization rather than one of partial melting of country rocks.

A group of isolated (7) late Carboniferous granitoids associated with the Peel Fault display features which distinguish them from other granitoids of the New England Batholith. They are characterized by low contents of K20 and related incompatible elements, very low initial 87Sr /86Sr ratios and they have textures which indicate rapid crystallization from a total melt. These criteria are consistent with a model in which chemically and isotopically primitive but amphibolitized ocean-floor basalts, believed to have formed in a marginal sea, are partially melted as the marginal sea floor was being subducted, presumably at the arc-trench gap. This model is further consistent with the occurrence of high-pressure low-temperature metamorphic rocks along the Peel Fault. 239.

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INDEX OF ROCK SANPLES

HILLGROVE SUITE SA11PLES

Sample Catalogue Pluton Rock Distinguishing No. No. Type features

HRA 46026 Henry River Adamellite adamellite K14 46027 Kookabookra Adamellite " SHKK 46028 " " sheared KKF 46029 " " eastern margin TOBA 46030 Tobermory Adamellite " WTOBA 46031 " " western margin ABGD 46032 Abroi Granodiorite granodiorite AB9 46033 " " AB6 46034 " " eastern margin WOLL 46035 Wollomombi Adamellite adamellite sheared RVGD 46036 Rockvale Granodiorite granodiorite RVKY4. 46037 " " RVTlO 46038 " adamellite northern margin RVT7 46039 " " ?dyke; fine-grained HGA 46040 Hillgrove Adamellite " HG270 46041 " " HG272 46042 1\ II HG273 46043 " " FHGA 46044 " " northern margin; fine-grained CT13 46045 " " Bakers Creek Gorge; massive LHGA 46046 " aplite Long Swamp Road CT5 46047 " tonalite xenolith HG271 46048 " " " DUND 46049 Dundurrabin Granodiorite granodiorite 11 FDUl.~D 46050 " western margin; fine grained DUNDX 46051 " tonalite xenolith LDUND 46052 " 1euco- felsic vein adamellite BKA 46053 Blue Knobby Adamellite adamellite ENA 46054 Enmore Adamellite " Vi S[:mple Catalogue Pluton Rock Distinguishing No. No. Type features

FENA 46055 Enmore Adamellite' adamellite fine-grained LENA 46056 " aplite eastern margin ELA 46057 Eastlake Adamellite adamellite ELAX 46058 II \I xenolith WBN24 46059 " " western margin WINT 46060 Winterbourne Adamellite " fine-grained KA 46061 Kilburnie Adamellite 11 KILB 46062 " " fine-grained INGA 46063 Ingleba Adamellite 11 ARG 46064 Argyll Granodiorite granodiorite ARGX 46065 II " xenolith BlO 46066 " " northern margin; roof facies CDK 46067 II " western margin TH2 46068 Tia Granodiorite II southwestern margin TI14 46069 " " LTH2 46070 " leuco- felsic vein adamellite GK6 46071 Garibaldi Adamellite adamellite

BUNDARRA SUITE SAMPLES

BS 46074 Copeton Adamellite adamellite fine-grained; porphyritic BS155 46075 II 11

NEW ENGLAND SUITE SAMPLES

KD 46100 Kentucky Diorite diorite very mafic KPD 46101 Kentucky Ponds Diorite gabbroic diorite C14A 46102 Wongalee Complex quartz diorite fine-grained BCKT2 46103 Back Creek Hicrotonalite quartz northern margin monzonite BCKT3 46104 II quartz fine-grained monzodiorite BCKT4 46105 " quartz " monzonite Sample Catalogue Pluton Rock Distinguishing No. No. Type features

BCKT5 46106 Back Creek Microtonalite quartz fine-grained monzonite SHT3 46107 Shalimar Tonalite tonalite eastern margin SHT2 46108 " " foliated SHT4 46109 " adamellite microporphyritic SIITl 46110 " " SHT13 46111 " " southern margin KT 46112 Khartou n Tonali te tonalite CQM If6113 Clovernook Quartz quartz Monzonite monzonite HGPT 46114 Harnham Grove }1icro­ micro­ tonalite granodiorite TVPT 46115 Terrible Vale Micro­ " tonalite WT 46116 Wilhelmshohe Tonalite tonalite UGD 46117 Uralla Granodiorite granodiorite FUGD 46118 " " fine-grained BGD 46119 Balala Granodiorite " GGl 46120 Glenburnie Adamellite adamellite LGGl 46121 " leuco­ very felsic adamellite

WRA 46122 Walcha Road Adamellite adamellite coarsely porphyritic HM208 46123 Highlands Monzonite monzonite HM207 46124 " " chilled margin WMA 46125 Wards Mistake Adamellite adamellite WQM 46126 Woodlands Quartz quartz Monzonite monzonite WQMP 46127 " adamellite porphyritic WQML 46128 " granite coarse-grained ORLA 46129 Oban River Leuco­ leuco­ adamellite adamellite RRAPL 46130 Red Range Adamellite aplite very felsic XENOLITHS IN NEH ENGLAND SUITE

Sample Catalogue Pluton Rock Distinguishing No. No. Type features

KTX2 46131 Khartoun Tonalite beerbachite KTXl 46132 " " WQMX 46133 Woodlands Quartz basaltic andesite Monzonite KPDX 46134 Kentucky Ponds Diorite biotite-rich beerbachite WTX 46135 Wilhelmshohe Tonalite monzonite ORLAX 46136 Oban River Leuco- quartz diorite adamellite GG2X 46137 G1enburnie Adamellite hedenbergite ? sediment hornfels UGDX 46138 Uralla Granodiorite quartz monzonite

SAMPLES OF TRANSITIONAL GRANITOIDS

BCT1 46080 Billys Creek Tonalite tonalite fine-grained BCTX 46081 " xenolith propylitized and kaolinized PAG 46082 Gostwyck Adamellite adamellite orthopyroxene- bearing GAl 46083 Gara Adamellite adamellite western part GA2 46084 " 11 eastern part GAX 46085 " xenolith fine-grained, darker LGA 46086 11 leucoadamellite felsic part MDA 46087 Murder Dog Adamellite adamellite RIGD 46088 Rockisle Granodiorite granodiorite/ western part adamellite ERIGD 46089 " " eastern part RIGDX 46090 " quartz-monzodiorite " Sample Catalogue Pluton Rock Distinguishing No. No. Type features

SANPLES OF Lm~-K GRANITOIDS

LHA 46091 Linden Hill Tonalite tonalite LLHA 46092 " leucoadamellite felsic segrega- tion BTGD 46093 Barrington Tops tonalite Granodiorite GTT 46094 Gogs Top Trondhjemite trondhjemite HTEG 46095 Mt Ephraim Granodiorite tonalite DCTI 46096 Duncans Creek Trondhjemite trondhjemite DCT2 46097 " " DCT3 46098 " "

SANPLES FRml THOLEIITIC MAFIC COMPLEXES

NPG 45956 l-1oona Plains Complex olivine gabbro high-Me RKE 45957 " gabbroic diorite D60 45958 " diorite western part EDI 45959 " " central part No.96 45960 " calcic " trondhjemite W8 45961 " olivine gabbro low-Me G3 45962 " gabbro low-Me; coarse grained EIT 45963 " biotite gabbro KVD 45964 " diorite eastern part MPT 45965 " quartz diorite KVT 45966 " quartz diorite eastern part NPGR 45967 " granophyre SGTR 45968 " quartz diorite southeastern part

II KA 45969 adamellite MFFA 45970 " " MFA 45971 " aplitic vein garnet-bearing; in KA MPTAP 45985 " " crosscutting BPT Sample Catalogue Pluton Rock Distinguishing No. No. Type features

19153 45972 Days Creek Complex hornfelsed roof, very fine­ (southern stock) gabbro grained 19131 45973 " " " D25 45986 " porphyritic fine-grained; gabbro eastern contact D8 45987 " hOr~tfe1sebdbPar-southeastern margin gasl e ga ro D9 45988 " hornfe1sed " gabbro D12 45989 " " II 19148 45974 " olivine gabbro coarse-grained cum­ ulate; low-lJG DCNG 45990 " hypersthene gabbro 19140 45975 " dioritic vein in 19131 227A 46021 " ?hornsfe1sed inner part of gabbro core stone D27B 46022 " gabbroic middle part of diorite core stone D27C 46023 " felsic diorite outer rind of core stone D32 46024 " II segregation in 19131 19142 45976 " aplite felsic segregation in 19131 D3l 46025 " II II WEN 45977 Woodburn Complex olivine gabbro coarse-grained; high-MG WB23 45978 " diorite GK2 45979 Apsley River Complex olivine gabbro fine-grained; high-MG GK4 45980 " II II GK3 45981 " II coarse-grained; high-MG GK5 45982 II II II BHC10 45983 Barney Houses Complex II fine-grained; 1m.;r-;'·:C BHC2 46140 " II II DMl 45991 Dorrigo Mountain microdiorite ?xeno1ith in DH4 Complex DM3 45992 " biotite fine-grained; microgabbro xenolith in DH4 Sample Catalogue Pluton Rock Distinguishing No. No. Type features

DMl 45991 Dorrigo Mountain microdiorite ?xenolith in D}f4 Complex DM3 45992 " biotite fine-grained; microgabbro xenolith in DM4

DM7 45993 Dorrigo }fountain Complex biotite microdiorite DM4 45994 i' granodiorite DM7V 45995 II felsic vein crosscutting DM7 DH8 45996 II felsic fine-grained adamellite FHB 45997 Bakers Creek Complex gabbroic diorite HC17 45998 " gabbro HGT2 45999 II biotite quartz diorite HGT3 46000 II " HC14 46001 " " BAK 46002 " " CHB • 46003 II microdiorite 'chilled margin' to gabbroic diorites HBX 46004 " " xenolith in BAK CC 46005 Camperdown Complex micro gabbro El 46006 Table Top Diorite gabbroic microdiorite TT3 46007 Mountain View Diorite biotite quartz diorite

NT 46008 Mornington Complex quartz diorite microdiorite v.fine grained MD 46009 " IMD 46010 " felsic vein LMD 46011 " " D2 46012 Shady Acres Complex microga~bro n D7 46013 gabbroic diorite CT 46014 Cheyenne Complex quartz diorite KR2 46015 Moggs Swamp Complex " n KR1 46016 " KRlV 46017 " large felsic central part of vein vein in JOKRGD outer part of KRLV 46018 " " vein in JOKRGD KRTV 46019 " small vein in JOKRGD JOKRGD " granodiorite northern part {;RJD.~ .. ___ l\i.FLRL:~CES . __ .. _ ... __OF._. ___F:UCKS . ______l::XAl·;n;ED . ____ 11;._. ______TillS THESIS . ____ ._ ..B:\SED_____ O:--l . ___ 1:. __ 250 . __ -1 __000

~E0L.0~_I..~L MAPS SH~~. __-=-_~L_9_Ll.9J_.1)_&_ 14

------_. Sample Catalogue Grid Sample Catalogue Grid No. No. Reference No. No. Reference

--'--'-~----'------lilLLC1WVE SUITE SAl'lPLES

BRA 4&026 5J1295 ELA 46057 465184 K14 /.6027 510282 ELAX 46058 466186 SliKK 46028 511283 l-,'BN24 46059 464184 n~F 46029 513285 \~INT '16060 484184 TOllA 46030 506260 KA 46061 445148 '..'TOEA 46031 496258 KILB 46062 444154 ABCD 46032 523245 INGA 46063 445143 A139 1.6033 523237 ARG 46064 497165 AB6 1,6034 522236 AI

TVPT 46115 1,49191 klGD 46088 443123 '",T 1.6116 445197 ERIGD 46089 445124 UGD 46117 455208 RIGDX 46090 445124 FUGD 46118 448207 SAhPLES OF LOi.J-K GRANITOIDS BCD 46119 43i)209 eel 46120 443195 LIlA 46091 454164

LGG1 46121 443195 LLHA L16092 454164 WRA 46122 436169 BTGD 1.6093 435056 lU1208 46123 476245 GTT 46094 434094 HH207 46124 475245 HTEG 46095 417102 w"MA 46125 494263 DCT1 46096 420115 WQM 46126 510282 DCT2 46097 420114 WQMP 46127 510283 . DCT3 46098 420114 WQML 46128 510283 SAl-fPLES FROM THOLEIITIC HAFIC 46129 ORLA 499277 COMPLEXES RRAPL 46130 499318 KTXl 46131 444207 HPG 45956 493163 KTX1 46132 444207 RKE 45957 492164 WQMX 46133 510283 D60 45958 492163 KPDX 46134 445196 ED1 45959 493163 WTX 46135 445197 No.96 45960 493163 ORLAX 46136 499277 W8 45961 492163 GG2X 46137 443195 G3 45962 492162 UGDX 46138 455208 EIT 45963 493164 KVD 45964 497165 SAMPLES OF TRANSITIONAL GRANITOIDS MPT 45965 493164 BeTI 46080 563267 KVT 45966 497165 BCTX 46081 563267 HPGR 45967 491162 PAG 46082 464204 SGTR 45968 495163 ------_.----. ---_._------.----- ._--- Sample Catalogue Grid S.:mp1e Catalogue Grid No. Nu. Reference No. No. Reference

SAHPLES FROM THOLEIITIC MAFIC CmlPLEXES CONT'D KA 45969 492163 DM8 45996 584235 J.1PFA 45970 491163 BIB 45997 495213 }lPA 45971 492162 HC17 45998 495213 l>lPTAP 45985 493164 HGT2 45999 495214 19153 45972 502259 HGn 46000 495214 19131 45973 502259 HC14 46001 495213 D25 45986 502258 13AK 46002 496213 DB 45987 501258 CHB 46003 495212

D9 LI 5988 501258 HBX 46004 496214 D12 45989 501258 CC 46005 514237 19148 45974 502259 E1 46006 482195 DCNG 45990 502259 TT3 46007 483193 19140 45975 502259 MT 46008 512268 D27A 46021 502259 HD 46009 512269 D27B 46022 502259 LMD 46011 512269 D27C 46023 502259 D2 46012 557265 D32 46024 502259 D7 46013 557264 19142 45976 502259 CT 46014 491187 D31 46025 502259 KR2 46015 510288 WBN 45977 464184 KRl 46016 510288 WB23 45978 464184 KRIV 46017 510288 GK2 45979 501150 KRLV 46018 510288 GK4 45980 501150 KRTV 46019 509288 GK3 45981 501150 JOKRGD 510289 GK5 45982 501150 BHC10 45983 478195 BHC2 46140 478195

SA}WLES FROM CALC-ALKALINE MAFIC COMPLEXES DM! 45991 584235 DM3 45992 584235 DM7 45993 584235 DM4 45994 584235 DM7V 45995 584235 APPENDIX II

ANALYTICAL METHODS

1. Sample Preparation

Most New England intrusions are extremely fresh and readily accessible, hence large samples (-10-20 kg) were usually collected for chemical analysis and mineral separation. During the removal of any weathered material, one or more samples weighing 0.3- 0.8 kg (depending on grain size and homogeneity) were selected for analysis. All rocks were crushed with a steel jaw crusher and ground to a fine powder (usually < 200 mesh) in a tungsten carbide Siebtechnick mill. The usually unsplit powders were stored in glass jars only.

2. Major Elements

Most of the major elements listed in the analytical tables were determined by X-ray fluorescence spectrometry using an automated Philips PW1220 spectrometer (A.N.U.). Some were determined at Adelaide University using a

Sieme~s SRSI fully automatic spectrometer. Si, Ti, AI, EFe, ~fu, Mg, Ca, K, S and P were measured in duplicate on glass discs prepared by the fusion method of Norrish and Hutton (1969). FeO was determined separately by dissolving the sample in a hot HF / H2S04 mixture and titrating against ammonium eerie sulphate using N-phenylanthranilic acid to indicate the end point. determined by the Penfield method; 0.5 - 1.0 g of sample in a silica glass tube was heated in a rod furnace at - 1100°C. The H20 was collected in a condenser outside the furnace. Sodium was measured on an EEL flame photometer using AGV, BCR and GSP as standards.

3. Trace Elements

The trace elements Rb, Sr, Y, Pb, Zr, Nb, were measured in duplicate on rock-powder pellets using the methods of Norrish and Chappell (1967). Mass absorptions were measured directly from pressed powders of the samples (at least in triplicate). A summary of analytical conditions for X-ray fluorescence spectrometry is given in Table A.l.

Trace elements in samples measured at Adelaide University agreed closely with those measured at A.N.U. For all trace element analyses single samples only were run. Mass absorptions were calculated from total-rock analyses except for Rb, Sr, Y and Th where the Ho Compton peak was measured. Except for some IU and Cr values obtained by XRF, most Hi, Cr, Zn, Cu and Li concentrations were lileasured using an AA 5 Varian Tech tron spectro­ photometer. Accuracy was monitored using AGV, HCR and GSP standards. Precision on duplicated samples was always better than 4%.

4. Sr Isotopes

Isotope dilution procedures and mass spectrometry techniques generally followed those of Compston (1965), Arriens and Compston (1968) and Page et aZ., (1976). Total-rock and mineral samples ranging from 0.02 g to 0.45 g (depending on their Rb and Sr concentrations) were dissolved and converted to chlorides using HF, HCl04 and HCl. Sr and Rb was concentrated via large and small anion exchange columns containing Dowex AG SOW resin. Sr and Rb blanks were near 0.02 Vg, which would result in errors of 87Sr/86Sr an order of magnitude less than instrumental error. Most Sr isotope measurements at A.N.D. were made by magnetic field switching on a Nuclide Analysis Associates instrument (30.5 em radius of curvature, 60° sector). Most Rb isotopic measurements at A.N.D. were made on a 15.25 cm, 90° sector MSX mass spectrometer. Both mass spectrometers employed 6 kV accelerating voltage, Faraday cup collector and Cary electrometer and were operated on-line to a HP-2ll6-B computer which also controlled the magnetic-field peak-switching. The remaining Rb and Sr isotopic measurements on biotites and low-level total-rock samples at A.N.U. were made using a 23 cm radius of curvature, 60° sector MSZ mass spectrometer described by Clement and Compston (1972). Analyses of NBS 987 strontium carbonate on the Nuclide mass spectrometer gave a ratio of 0.71032 ± 6. Rhenium triple-filament sources were used except for biotite measurements at Adelaide University where a single­ filament tantalum oxide source was used.

All Sr ratios were corrected for variable mass discrimination by normalizing 88S r /86Sr to 8.3752. Mean experimental uncertainties for 87Rb/86Sr and 87Sr/86Sr are estimated to be 0.5% and 0.2% respectively. Regression of the data is based On the work of McIntyre et aZ. (1966). All uncertainties in this treatment are given at 2 sigma. The value used for the Rb decay constant is 1.42 x 10-11 y-l •

Total-rock samples were also analyzed for Rb and Sr by long-count X-ray fluorescence technique,generally following the procedure of Chappell et aZ. (1969). Three powder presses of each sample were each analyzed three times. Results were calibrated against the reference standard NBS 70A (522 ppm Rb and 65.3 ppm Sr). 5. Electron Hicroprobe

Minerals from thin-sections, lnounts and concentrates were analyzed by energy-dispersive TPD-microprobe following the procedures of Reed and Ware (1973, 1976) and Ware and Reed (1973).who also give the limitations of this method. Anhydrous minerals were normalized to 100% for comparative purposes.

\ I' I L"' !