Permian Castile Varved Evaporite Sequence, West Texas and New Mexico

Home , Bell Canyon Formation, Castile Formation

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Reference 14

Anderson, R.Y., Dean, W.E., Kirkland, Jr., D.W., and Snider, H. I. 1972. Permian Castile Varved Evaporite Sequence, West Texas and New Mexico. Geological Society of America Bulletin, Vol. 83, pp. 59-86.

Submitted in accordance with 40 CFR 8 194.13, Submission of Reference Materials. SENT BY: 2-28-96 ; 4: 08PM ; WID - PRmm7fT3602: @91;115434 6541 ;# 2/ 8

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6 715LO-OOU3 PCIPLI~TTON,nwu. -, P SOECC . ag)PPIlf. 0.11. '917 snrmon ~~RUSTRYOT w nmrmmxxcA rrrra- VOL. 3 AuDanIC Paas 12so ~mam. SABl DIEOCI, CA 92101 ME 1619) 699-6321 N~OZOO 7 71510 00173 10.00000 Eb 11.000 P. lAO.00 PQRLICATIOU, 800Us. W(IP1~8.YIYIRILPILT. sxa wo2.B YQY SPOCS . ..- cbnrinuma on uut. p.9. =k=-L-s=me W ROGER Y. ANDERSON Deporrn7eric of Geology, The Unizersity ofNew Mexico, Albuqrrerque, h'eru Mexico 87/06 I!'AL?'ER E. DEAN, J I<. Deparrnrer~rojCeology, Sj'roruse Un~rrrsify,Syracrrse, New York I3210 I)OUGLAS 11'. KIRKLAN D AfoPil Research and Dezriopmenr Corpornrion, L)alIas, Texas 75221 IlENRY I. SNIDER L)epartn~crrtof Ph~sicnl Scicrlces, Eastern (Jotmectic~~tStare College, ti'iIlimanric, Cormnectirrrt 06226

West Texas and New Mexico

is a change from thinner undisturbed anhy- (lritc I:IITI~II:I~ to 111icI

sedimentation-a varve. tl~ickestin the cnstcrn and northeastern part of l'lic thickr~essolrncl~ couplet iu tllc 260.000- 111c11;lsirl :tn~ltl~ickcl~ from southcast to nor111- varvc scclrrrllcc (:I total tllicktlcss 01 447.2 In, west. 'l'his distribution and the synchroneity 1457 It) I~asbccn measured individ~rall~and indicate a departure froln the classical model of recotded and provides the hasis for subdividing cvaporirc zonation. and corrclatir~g111:1ior strntifir:~pI~ic units witllin INTRODUCTION tile basin. 'l'hv ul)l>crruc~st9.2 111 (30.3 1t) 111- the Bell Car~yor~Formation contains about 50,850 The Castile Formation (Upper I'ermian) in varve co~~plets:the Basal Limcstonc hternber the I>elaware Basin of Texas and New blexico of the C:atile about 600; tl~elowermost anlly- is oftcn cited as perhaps the best example of a drite mcrnbcr 01 rhc Castile (i\t~hytlritc1) con- large dccp-water evapc~ritedeposit k~rwhich tnins 38,397: 1l:llire 1, 1,063; Anhytlritc 11, tl~crcarc 11o tntdcrn :itlalogs. In ;tdditiol~,rl~c 13.314; Il:~licc11, 1,758: ~I~~hyclritcIll, 46,592: <::~stilc is \vcll knolvn Ii~rits rcil~nrk:lbly tlis- Iblitc 111, 17,870; ;r~xlAr~l~~tlritc IV, 54,187. ti~~cr1:uninntions ol calcite and ;tnhydritc, The part of the Salildo collccrcd (126.6 111) cou- \vhicl~are assumed by Illany to rellect annual cains 35,422 vnrvc couplets. 'l'llc Bell Canyon- sedimentation. Gstilc scqnencc in the cores studied is appar- 'l'he rcgular interlamination of salts of dif- cnrly continuous, \\!it11 no recognizable uncon- ferent solubilities (calcite and anl~ydrite;anhydrite and I~alitc)implies that depositional con- l'he dominant petrologic oscillatiot~ in the trols must have fluct~~atedin response to some Castile and Salado, other tllan the la~ninations, peritdic proccss or event. Udden (1924) sug-

PPICMIAN CASI'ILE EVAI'ORITE SEQUENCE, \\'EST TEXAS AND NEW MEXICO 61 gested tlint c;lcl~ calcite-an11)-drite couplet tliors (Anderso~iand Kirkland, 1966; Kirkland represented an annual increment of sediment- and Anderson, 1970) revealed that the lamina- a varve. hlost investigators wlio have discussed tions could be correlated with great precision the Castile agree \vith Udden's annual inter- over the entire basin (distances up to 113 km or pretation I~uthave bee11 urlablc to agree on a 70.2 mi). The laminations continue in an unin-

Or~iitlly1-11 :yrr :~sciII 111c cvnporilc system and considers chicfly the calcite I;IIII~II;I~ ill 111c Casrilc. Kicllter-Bern- pcrl.ology and s~mtigraphic relations ol the burg (1964) explained a similar association in major units in the basin. These units have been calcite-anhydrite couplets in the Permian correlated within the basin on the basis of ANDERSON AND OTtlERS

REGIONAL SETTING

the basin. During Salado time, potassium salts were dcposired rvitllin southeastern New Mex- ico and a small part of Texas.

PETROLOGY Castile - The laminations of the preevaporite and evaporite phascs of Bell Canyon-Castile For- Guada'upe mations provide a unique means for describing Cherry tanyon and intcrpreting petrologic variations. Lamina- Brushy Canyon tions of onc sort or another occur in a continuous uninrerruptcd seclucnce Itom the Leonard Bone Sprlnq ~imstme organically lamina ted siltstone of the Bell Canyon, through the basal limestone and the

. ., 8,. ,). . ._-- . ______.. . . _. _- _ . -- - - . -- - -. -- .-

PERMIAN CASI'ILE EVAI'OIIII'E SEQUISNCE, WEST TEXAS AND P:EW MEXICO 63

; of thc (::~srile, anti

i .\nliytlrite 1, -1.0 $.

.. Icr~~ber.

111 I:~ycrs:I\)OIII I mrn

the Castile Formation, and some additions to and refinements of these descriptions are pre- I OF PERMIAN ROCKS OF THE :I0 SOUTHEASI llEW MEXICO -

'rdbeds

,#yon

;.I Limestone scrvcd wit11 six or more calcite rl~ombsarounda Some basal calcitc laminae contain a mosaic nucleus ol calcite or unidentified material. ltlated of equidimensional calcite crystals with many The size of the small equidimensional calcite of the crystals having sutured bor~ndaries. As rhombs does not change upward in the laminae lypical of most of tlic Castile. lollg tli~~~c~~sionsor no st arc :~pproxin~a~cly I\NI)EI

Figurc 3. Fossils in thc uppermost BcU Canyon 50.3 cm. (D) Small (-25,~) calcitc rhombs in Formation and crystal tcxturcs in thc Castilc Formation. laminae ncar basc of Anhydritc I (see Fig. 2G); (A) Roundcd-rhombohcdrons of calcitc; note that thc organization of calcitc crystals into lamina in ccnt frcqucncy of calcite crystals diminishes upward into the photo. (E,F) Enlargcd vicws of calcitc rhom overlying anh~dritclamina, Anh~dritcI Mcmbcr, To partially polarized light; notc that somc crystok + 10,792, 859.9 cm. (B) Algal(?) rcmains, Claystonc rhombic form and arc "floating" in anhyddtc 111 unit, To + 5,600, 74.3 cm. (C) Minute fusulinid, mass. comparc Yubrina sp., Claystonc 111 unit, To + 3,840, PERhiIAN CtISl'ILE I

A lmm

F -lmm Figurc 4. Calcite and ar~hydritccrystal tcxturcs, 35,014-35,015. Notc that organic matter forms a coating Castile and Salado Formations. (A) Anhydritc and on thc calcitc grains. (D) Calcitc rhombs (dark) bctwccn I hombs in calcitc organic-rich anhydritc laminae (scc Fig. 2F); notc con- nodulcs of anhydhc; notc alignmcnt of anhydritc t, Fig. ZG); note trasting sizc of anhydritc crystals, with larger crystals in crystals adjacent to calcite band, Anhydritc I Mcmbcr, ltrlina in center of organic-rich zones (polarized light); Anhydritc I To + 216-218, 35.6 cm. (E) Similar to (D), but in :~lcitc rhonrbs in Member TO+ 21,630-21,631, 2,195.6 cm. (B) Typical polarized light, Anhydritc I Mcmber, To + 216-218, rrr crystals retain 1 blocky anhydritc (polarizcd light); Anhydritc I Mem- 35.6 cm. (F) Rcticuhte pattern formcd by rcorganiza- 1 :,rll~ydritcground bcr, To + 13,976, 1,200.0 cm. (C) Laminac of organic tion of anhydritc laminae into nodules, Anhydritc I stained calcitc and anhydritc, Salado Formation; Mcmbcr, To + 216-218,35.6 cm. 12,737.8 cm above basc of Salado Formation. TO +

Some of the halite layers from the upper part of laminae. They can be observed in insoluble theCastile retain the original crystal structures, residues and sometimes on polished surfacesand '~ir~etersto IllOle including internal laminae that are concentra- in thin sections, but are observed best on x- \ added to the tions of organic material or anhydrite, and radiographs of slabs approximately 3 mm thick rn at the onset bubbles and vacuoles. Most halite layers, Ilow- cut normallv to stratification (see discussion in ;I 1 tlrite 1.1rninac ever, have become recrystallized (Fig. 5D). Anderson aid Kirkland, 1966): I( Lrl~essR 1111 the Very small quartz and zircon grains with Other Components 1 r jlcire laycrs be- maximum intercepts of approximately 50 p I 8 lcfined nnil arc Small crystals of pyrite are sparsely present have been observed in insoluble residues of in the Cistilc, gcr~cmlly:~t thc basc of calcite Castilc material. Tllcir quantity has not been

. .

UNION -UNIVERSITY UNIVERSITY OF NEW MEXICO "37" no. 4 PHILLIPS no. I VARVE THICKNESS

BELL CANYON FORMATION SILTSTONE rn

Blanket solution breccio (vorve thickness estimated1

- 1 -

ll.lIl\N \sllll: l.\\0llsl;ull, \\I ll\ AN I IIO 73

*fllc l~rccci:~gcncr:llly corisists rdrcct;lngl~lar- probably extend over rnost of the Delaware shaped, sr~l);~rlgul:~rl'r;~g~licrl~s oI'sirlglc i;umillac Basin and Ilave bccn subdivided into six work- gro111)s01' I~IIII~II;I~c111l~c~I~lc~1 111 :I 111:ltrix 01' i11g 1111its..I'lic type scctioti for the stlbdivisio~i anllydritc (Fig. 5C). 'I'lic hgmcllts, gcncr;lIly is :I tnrtial core irolli tllc Ulmion-University less than one clii in Icllgtll, occur in various "37" 110. 4 supplc~iielltedby a sonic log, l'rolml orientations, but rnost occur with str:~tificaticln. ~vliich correlation call bc made tiirotlgliot~t if visible, slid lo~igdimension near tlie liori- 111ost ol the basin. /In additional supplement to zontal, hln~iyol tlie fragrnc~~tsappear to llave tlle type scctio~m is the University of New been only slialltly tlisl,l:lcctl. klcxico-l'liillips ~io.1 core, which includes the 111 solnc ol' tlic L~lankct brccci;~I,ctls it is elltire Castilc Forination and can be co~isidercd difficult to correlate ~llcupper contact bccause a "master" or "type" time series for the basin. of solution collapse that resulted in a collapse- The relation between these two sequences and type breccia (Fig. 513) co~lsistillgof larger. position of members is sllown in Figure 6. The more angular lragliielits than the blanket solu- number and average thickness of varves in each tion breccia. and \virli little matrix. Good ex- unit are given ill Table 2. a~nplesof collapse-type breccia Iiave been oh- Upper Be'1 Canyon Formation served at the top of tlle Halite I1 AIelnber and in the upper part ol the Anhydrite I\'Atember The upper part of the Bell Canyon Forma- above blanket solution breccia. tion can be subdivided into a number of units, Siltstone I through Claystolie 111 (Fig. 6), SUBDIVISION AND DISTRIBUTION n4micli are correlative over a large part of the OF TIE CASTILE AND UPPERMOST DelawareBasin. BELL CANYON FORMATIONS The siltstone and claystone units of the up- The Castile Forrn;ltion llas been subdivided permost Bell Canyon varved sequence are here into eiglitl members ivliicli permit eaami- easily recognizable in the cores from the nation of tlie present arc:ll tlistril~~ltion[,:Itterns western part of tlie basin, but they are not as of halite :lnd :~nliytlritc.Siltstonc and claystolie \\.ell dcIi~iedin tlie core lrom time eastern part. units in tlme rlppcrlnost Bell Callyon Fornmation -1'here is excellent correlation of laminae in

VNrePhilllps bl Nuder of Average thickness of Form t l on varve couplets Thickness calcite-anhydrite varve couplets

Salado Fom tion 35.422 12.660 cm 0.36 cm (partial sectlon. undifferentiated) -Henbers Castile Fornatlon Anhydrite IV 54.187 9,842 cm 0.18 cm Halite 111 '17.879 2,748 cm 0.16 cm (including anhydri te beds) Anhydri te I11 46,592 9,554 cm 0.21 cm Halite 11 t 1,758 801 m 0.45 cm (including anhydrite beds) Anlrydri te 11 14,414 2,733 cm 0.19 cm Halite I t 1,063 330 cm 0.31 cm Anhydrite I 38,397 5,092 cm 0.13 cm Basal Limestone 600 28 cm 0.04 cm Estlmted totals (Castile Fannation] 174,890 31.133 cm Average thickness of (In(ts clastlc-organic varge couplets Bell Canyon Formation Claystone 111 5,000 78 cm 0.01 cm Siltstone Ill 24.814 551 cm 0.02 cm Claystone I1 15,650 166 cm 0.01 cm Slltstone I1 1,086 44 cm 0.04 cm Claystone I ttca. 2.000 24 cm ca. 0.01 cm Siltstone I ttca. 1,500 61 cm ca. 0.04 cm

Estimated totals (Eel1 Canyon Fomtion) 50.850 924 cm Chlned totals 261 .I62 44.717 cm -- NWr of layers In halite fraction determined by extrapolation. t Nunber of layers deternined in Union-University "37" 14 core; thickness of calcite-anhydrlte fractions only. tt Nu*r of layers In UNMowden 14 core. 74 r\NDEI

these units bet\veen the Phillips no. I and isopach map constructed chiefly frorn sonic logs Cotvden no. 4 cores, a distance of 24 kln (Fig. (Fir. 10). rI'lie thickness is a fairlv constant 170

carbonate than tile I'hillips no. 1 section. (106.7 m). Anhydrite I becomes more calcarc- Laminae in the siltstone-claystone units in orrs in the southrwstern Delaware Basin tlie Union-University "37" no. 4 core are (Adams, 1944) and thickens radially to the about the same thickness but with less siltstone north and east frorn this area. and more carbonate tl~anin the Pliillips no. 1 Tlle continuity of laminations within the and Cowden no. 4 cores. Onlv a two-ft (0.61 Anlivdrite 1 Alember and other anhvdrite

Tile '~amarLimestone Aiember of tlie Bell llA and B show photomicr&raphs of ;hi" Canvon Formation interrupts the Clavstone 11 sections of correlative intervals with a north-

no. I and Cowden no. 4 cores but are more that comprise the laminations. The three com- nlrnicrous and tliickcr in tile Phillips section. A pl~nentscan be separated from each other by Ccw si~iiiI;~rli~iics~r~~ic beds several cc~itilnctcrs s:~lnl)lingslid analyzing the material on a uni~ tliick are also fou~itlbelow Siltstone 111 in the time basis (see Anderson, 1967; Kirkland and U~iion-University "37" 110.4 core on the other Anderson, 1969). Correlation cwfficients for I side of tlie basin, but it could not be deter- the percent of cach component in 10-coudct

Castile Formation Basal Limestone Member. hlany evc~porite

I 11 stone Alember of the Castile, however, is very !?!

anhydrite, extends throughout much of the -- Delaware Basin and was recognized as a distinct

in tlie University "37" no. 4 about 50 cm. The unit colisists of about 600 calcite-orea~liccou- 11 --- 3 z., .. . 1 ! . plets. It is co~lsidercda nicmber because of its :)--'"-- 0.3mmi .. . --.*.--. 2 distinct character and persistence. An isopach V; COWDEN 4 . .. . F~~~~~ 9. Lami n--. ."---~ hj map was not constructed because the unit can- 3 5; not dclinitely be dclinlited on wire-line logs. s,ctions o6 uppel i;$ Anhydrite I Member. 'I'he tliickncss distri- Quanz silt lamime ; bution of the lowermost anhydrite unit, which matter (dark); SiItsto -- contains about 38,000 couplets, is shown by an 229.5-230.5 cm.

ANI)I

ward within the un Cowdcn cores which are separated from each samc thickness proportions and gene other by 14 km (8.7 mi) in a north-south pearance (for example, contact relations, direction. This difTerencc in continuity with over the I13 krn (70.2 mi) distance. direction in the hasin is best illustrated in the parts of the sequence have couplets WII WON - UNIVERSITY "37" NO 4 POKORNY NO I '

Ibr0lut. carbaute hsolutm oqmtc i hroluta sulfate 11 - 95; 991 cmfldace

I Valueslined. whichThtcbers are statvalu laminae; 'yrccnt arb i dated& by lms on I ganic. adsulhte ucr I prwnt nlw by cwl

I I

! POKORNY NO I II PHILLIPS NO. I i Couplet ~~~C~WSSS I ....&-~*r;;iT .. I -- i

II = 28; 991 cmftdenc* I I i I I I I I I'lClZhll~\N C:\S'I'II,II I;\';\I'Ol

' it.nt k)~.couplet tllickncss ~,rojx)rtions sr~ficicntl~diftercnt Il:~litc I rhickcns gradtlally Irom sotrth to ,. cores (Fig 12). tomakc 1;11nin;11)). lanlin;~corrclatiol~ extremely north in the eastern part of the basin and has a I nortl~nrst-south- dificult, altllo~r~lithc loliger trends and more ~rl:~simumtl~ickness of Illore than 400 It (122 ' I hick~\~:rrtrend variable couplcts can bc rcadily ~llatched(Figs. In) in Lea County, New Mexico (Fig. 13). ) ~llusttatcclhy the 7B and 1 IC). hlost 01 tllis nortl1n':lrd thickcnillg is probably

I !c;Llur 10. Halite I Member. 'l'lle Ion.cr~lrost halite clue to all illcrease in thickness ol individual I lies Ila\rc not yet lnember ol the Castile is the tllickcst and most laminae judging lrom tlle near synchroneity of I 'o~rlpnrly- Univer- extensi\.r 01' the (:astile I1:1litc units. 111 tllr 11;llitc clrl)o.rition ill tllc castcrli anti tvcstclll I :\(, (.;ISI(.I11 ~nrtof Ll~~ivrr~i~~"<7" 1111. ,I C.III(.,IIIC I l:~litr I 1l;lrts 01 IIIV l):~si~i(l:ig. 7A). b!vc11 i(I1alite bc- 1 IIV tllc r~ol)c~.nlost c~lcOI~IIS 1.3 0 111idric-;lit gan 200 yrs earlier in the north i I~!,drite 1. Strat- couplets tvitll an average tllickness 01 3.1 cm. than in the University of New hlexico- I Ininae, Iluwever, l'lle a~lllydrite-halitecoul)lets arc thickest at I'hillips no. I core, this would mean an annual I 1.1ir1parts of the the base ol Halite 1 and decrease gradually up- deposition rate ol as much as I0 cm (3.9 in.) of 1 ~nostexactly the ward within tile unit. halite ill the northern part ol the basin. The I :~ndgcnrral ap- origill:~l thickllcss ol I lalite I in the western TABLE 3. CORRELATION COEFFICIENTS FOR SAWLES I I ucl:~tio~is,color) 10-COUPLET plrt of the basin cannot be determined. Tlle Is . FROM ANllYDRlTE I. T + 33,921-34.871 FROM COUDEN 2 j I cllstancc. Other COYDEN 4, AND PHILLIPS CORES OF THE CASTILE FORMATI(IH tl~icknessoltlicsolutioll brecciazoneequivale~lt to i c. ~~,~~~lctswith tlle II:llitc 1 is :~l)out330 cni in tlic l'hilliI)s Cowden 2 Cowden 2 Cowden 4 110. ;111(1 vs. VS. vs. 110. I. <:OW(ICII 2, COW~CIIno. 4 cores Varlable Cowden 4 I'hlllips Phllllps :111d all that can be determined about the past thickness of halite in this area is that enough 1 PHILLIPS NO. I Quplet thickness 0.77 llalite was interstratified with anhydrite Percent CaC03 -0.54 -0.52 0.51 lalninae to cause brecciation upon solution. Percent organic

krolute carbonate 0.29 Msolute organic Mtolute sulfate

N 95; 99% confidence Iim\ts = t0.27

1):1rt ul tl~el):~siii ;III(I about 115 ft (35.0 m) tliick ill tile Union Oil Company-University Cowden Cowden Cowden "37" 110. 4 core. '1.l1e halite is interrupted by VS. VS . VS- live beds of carbonate-laminated anhydrite, Variables Cowden 4 Phillips Phillips ranging from a few centimeters to over I m Couplet thickness 0.99 thick that can be observed readily on sonic logs. 0.99 'l'lie cntil-c 1l:llite II blember including the percent organic -0.01 0.81 -o,Dg co~~l)lctsill thc :trlliydrite beds encompasscs 1758 +_ 10 couplets of whicli about 1139 +_ 10 Percent CaS04 0.99 0.99 0.99 :Ire :~nhydritc-hali~cand the otliers calcite- Msol~teCaco3 -0.93 0.94 0.95 :~~lIiydritc.'I'hc average ~l~ickncss(>[ thc halite- &solute organic 0.55 anhydrite couplets is 2.3 cln with the thickness Msclute CaS04 -0.99 0.99 -0,99 decreasing gradually upward within each halite unit between the live laminated anhydrite H ' 28; 99% confidence limits = t0.50 beds. irisham no. 1. (C) Values which are significant at the 99% level are under- lined. Thickness values are sunmations of 50 individual -I'he same five beds of laminated anllydrite 1 calcite (dark) and couplets; percent carbonate. organic, and sulfate were O~~~~rbetween breccia beds in the I'hillips no. 1 ,~iversity"37" no. determined by loss on ignition; absolute carbonate, or- t~illipsno. I. pnjc. and sulfate were calculated by mlttplying the corc, l)~ttllc relation is vague in the upper few 1 percent value by couplet thlckness. lcc~of brccci;~because ol faulting and collapse.

1'1;KbLIAN CiiS.I.ILIC LVA1'ORL.I.E SEQUENCE, \VEST TEXAS AND NEW MEXlCO 79

COWDEN 4 vs PHILLIPS I

COWDEN 2 vs COWDEN 4

34$320 years TIME

- - --

-~ I1liKh.flAN (:~\S'l'Il~l~1<~~.\1'01<[1'1: SI:(>UI

' I

OF STRATIGRAPHIC UNITS A comparison of the isopachs of the Anhy- . The intcrprctation that brcccia beds in the drite I and LL and the Halite I and II Members University of New Mexico-l'hillips no. 1 core reveals that halite gradually thickens toward represented halite beds in the eastern part of the north-northeast with a trend that differs

I'ERh4IAN CASTILE EVAPORIT13 SEQUE:NCE, WEST TEXAS AND NEW MEXICO 83

by about 90' from the anliydritc trend. Com- tion. The so-called ripple marks (Lang, 1937; parison of lamin;ic at thc base or 1Ialitc I and I'orch, 1917) are not sedimentary structures, Halirc 111 in t11c Union-Utiivcrsity "37" corc \)tit arc ~ninortectonic leaturcs that originated in Winklcr County :irirl tlic same 1arnitl:lc in after co~isolidatio~i(Kirkland atid Anderson, thecowden cores in the west-central part or tlie 1970). The nodular beds in the Castile, while basin, a distancc of 1 13 km (70.2 mi), shows a si~pcrficiall~resembling the nodular beds 15- and 27-yr difference in the onset ol llalite associated with tidal flat sedimentation, are deposition (Fig. 7). closely associated with normal varving and in Halite and anhydrite beds within [Ialite 11 fact are varved themselves and show no primary appear to sllow the same degree ofsynchroneit y. breaks in the continuity of sedimentation. It is more dificult to observe the end of halite Estimates of the depth of water have deposition in major units owing to collapse of ranged from 150 to 700 m (King, 1934; Adams nonbrecciated laminated anllydrite im- and Frenzel, 1950; Adams, 1944; Kroenlein, mediately above solution breccia, but judging 1939) and are based chiefly on the present-day from correlations of individual anliydrife beds rellef between the top of theCapitanFormation witliin 1l:llitc I I, npproxi~nntcly tllc snlnc (tllc "rcel") and tlie base of the Castile. number ol lalninae arc i~lvolvcd,suggcsti~lg Ncwcll atid o~licrs(1953, p. 189) and Adams that the end ol halite deposition in dilTerent and Frenzel (1950) discuss this method. parts of the basin was also nearly syncl~ronous. Ideally, the depth of water within an evap- The syncllroneity of halite depositio~~and orite basin should have little efect on the the markedly difTerent trends for halite and precipitation process (Schmalz, 1969) and the nnhydrite, suggest that the classical model of accumulated sequence should reflect changes in I evaporite salt zonation, as described, for environmental conditions of the water body. example, by Scruton (1953) must be modified In tlle Castile sequence, however, there is a progressive change in the proportion of mate- lor the Delaware Basin. Some lateral zonation ! exists, but factors that triggered llalite deposi- rials over an interval of several hundred thou- tion seem to have affcctcd almost tllc entirc sand years. basin si~ntlltancor~sly. Within the tliree halite members, lor 'I'lle isol~acl~III;I~S of tl~cAt~hyclritc I atid 11 cxalnplc, intcrcalatcd bcds of halite and anhy- Members indicate a thickening lrom west to drite become more and more common higher east in the form of a fan-shaped wedge. The in the formation. Halite I is a single bed of fanlike shape is best illustrated by the 175 ft halite. Halite I1 is interrupted by five thin contour in Anhydrite I and the 90 ft contour anh~dr~tebeds and Halite 111 by six major in Anllydrite 11 (Figs. 10 and 14). According anl~ydritebeds. In addition, the time series to basin reflux models of King (1947) and plot of couplet thickness (Fig. 6) shows a Scruton (1953) the thickness of a particular progressive increase in the amplitude of a evaporite facics sllould thicken radially from dominant oscillation in sulfate thickness that the marine connection. Il this is the case for Iias a frequency between 1.000 and 3,000 years the Delaware Basin, then the distribution (conzpare, for example, the tendency toward patterns of anhydrite in the Castile suggest oscillation in Anhydrite I and IV). that marine water entered the basin from the These progressive changes within the basin west over or through the reef, rather than from could be attributed to prolonged trends in the south as suggested by Kroenlein (1939), climate or sea level or they could simply be the King (1942) and Adams (1944). The halite result of a progressive shallowing of the basin distribution patterns would favor tllc inter- and tile increas~ngimpact of climatic change or pretation of a southern source but inasmuch as freshening upon a smaller water volume within anhydrite represents about 97 pcrcent of the basin. Castile time it may be more reasonable to look lor an alternate explanation for the diflering CONCLUSIONS halite distribution. The lamination (varving) process began prior to evaporite deposition and continued BASIN DEPTH uninterrupted throughout the deposition of a No sedimentary features observed or re- basal limestone member, four anhydrite ported from the Castile Formation can be members, and three halite members of the construed as evidence for shallow water deposi- Castile Formation. IndividuaI laminations 84 ANDERSON AND OTHERS

persist laterally for 113 km (70.2 mi) and New Mexico: Am. Assoc. Petroleum Gcologiq probably extend throughout the basin. Bull., v. 28, p. 1592-1625. The calcite-anhydrite laminations that are -1965, Stratigraphic-tectonic development lypical of the Casrilc changcd character during Dclawarc Uasin: Am. As=. Petroleu times of high sulfate deposition. 'She same Geologists Bull., v. 49, p. 2140-2148. thick anhydrite layers developed into beds of ---1967, Semi-cyclicity in the Castile Evaporir in Elam, J. G., and Chuber, S., eds.. Cycl ntdular anhydrite after formation; nodular scdimentn~ion in the Permian Basin: We I;~nii~~acand zoncs are also correlative witlli~~ 'I'cxas Ccol. Soc. Symposium, p. 197-203. the basin. The e isodes of high sulfate deposi- Adams, J. E., and Frcnzel, H. N., 1950, Capita tion or nodule Bevelopment are separated by barrier reef, Texas and New Mexico: Jou 1,000 to more than 3,000 laminae couplets. Geology, v. 58. p. 289-312. Halite deposition in each member was of Adams, 1. E., Frenzel, H. N., Rhodes, M. L., an short duration (1,000 to 2,000 yrs) and the Johnson, D. P., 1951, Starved Pennsylvania timing of deposition was in response to the Midland Basin: Am. Am. Petroleum Geo: same changes that produced thick sulfate ogists Bull., v. 35, no. 12, p. 26W2607. Adams, S. S., 1967, Bromine in the Salado Forma laminae. Halite beds originally extended tion, Carlsbad Potash District, New Mexic. throughout the basin and are represented now 1Ph.D. thesis]: Cambridge, Harvard Univer by blanket beds of solution breccia in the sity, 202 p. ~vcsternpart of the basin. Anderson, R. Y., 1967, Sedimentary laminationsir Anhydrite members of the Castile thicken time-series study, in Mcrriam, D. F., cd. eastward and halite members thicken north- Computer applications in the earth sciences ward, with a trend difference of about 90'; the Colloquium on time-series analysis: Kansa onset and end of halite and anhydrite deposi- Geol. Survey Computer Contr. 18, p. 68-72 tion is nearly synchronous over 113 km (70.2 Anderson, R. Y., and Kirkland, D. W., 1960 Origin, varves and cycles of Jurassic Todiltc mi) and probably over the entire basin, sug- Formation, New Mexico: Am. Assoc. Pctm~ gesting that the classical model of evaporite leum Geologists Bull., v. 44, p. 37-52. zonation must be modified for the Castile -1966, Intrabasin varve correlation: Geol. Sac. sequence. Also, influx of water into the basin America Bull., v. 77, p. 241-256. was apparently from over or through the west- Briggs, L. I.,1957, Quantitativeasptctsofevaporitc . ern reef or platform. deposition: Michigan Acad. Sci., Arts and A progressive upward increase in episodes Letters Paper, v. 42, p. 115-123. of halite deposition and an increase in the Carpelan, L. H., 1957, Hydrobiology of the AluLo fluctuation of sulfate deposition with time sug- Salt Ponds: Ecology, v. 38, p. 375-390. Carrozzi, A. V., 1960, Microscopic dimentar). gest a prolonged and sustained change in petrography: New York, John Wiey ,and environment or progressive shallowing of the Sons, Inc., 458 p. . basin. Hills, J. M., 1942, Rhythm of permian Seas,'.; paleogeographic study: Am. k.'Petrdcum Geologists Bull., v. 26, no. 2, p. 217-255. , " ACKNOWLEDGMENTS King, P. B., 1934, Permian stratigraphy of trans- The coring, data collection, and lab operat- Pecos Texas: Geol. Soc. America Bull., v. 45, ing expenses have been supported by the Earth p. 697-798. -1937, Geology of the Marathon region, Texas: Sciences Section c~f the National Science U. S. Geol. Survey Prof. Paper no. 187, 148 p. Foundation. The work of Dean and Snider --1942, Permian of west Texas and southeastern was partly supported during tenure as National New Mexico: Am Assoc. Petroleum Geologists Aeronautic and Space Administration trainees. Bull., v. 26, p. 535-763. ?'he authors are indebted to William T. -1948. Geology of the southern Guadalupc Holscr of the University of Oregon and to Mountains, Texas: U.S. Geol. Survey Prof. Chevron Research, Standard Oil Company of Paper 21 5, 183 p. California, for contributing slabs from the King, R. H., 1947, Sedimentation in Per,*. Union Oil Company-University "37" no. 4 Castile sen: Am. Assoc. Petroleum Gdoeisu" Bull.. v. 31, p. 470-477. cores, Winkler County, Texas. Kirkland. D. W.. and Anderson. R. Y.. . 1969.. Corn. pasition and origin of it; Blanca varvcs, b Andemn. R. Y., and Kirkland, D. W., A, REFERENCES CITED Paleoecology of an Early Pleistocene lake on Adams, J. E., 1944, Upper Permian Ochoa Series of the high plains of Texas: Gcd. Soc. 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8 1. I,., and Valley of New Mexico arltl 'I'exas: Am. Assoc. p. 510-519. I\\Ivania11 I'etrolcurr~ (;cologists Bull., v. 21, p. 833-898. Schmalz, I<. F., 1969, Deep-water evaporite deposi- 11111 Geol- Lloyd, E. R., 1929, Capitan 1,irnestone ancl asso- tion: A generic model: Am. Assoc. Petroleum 1>07. ciated formations in New Mexico: Am. Assoc. Geologists Bull., v. 53, no. 4, p. 798-823. 10 1:ornla- Petroleum Geologists Bull., v. 13, p. 645-657. Scruton, P. C., 1953, Deposits of eva~orites:Am. I\. hlexico Maley, V. C., and Muflington, I<. M., 1953, Assoc. Petroleum Geologists Bull., v. 37, no. tl Univer- Cenozoic fill and evaporite solution in the I I, p. 2498-2512. Delaware Basin, Texas and New Mexico: Geol. Skinner, J. W., and Wilde, G. L., 1955, New illations in Soc. America Bull., v. 64, p. 539-546. fusulinids from the Permian of west Texas: . I:., ed., Mutch, T. A., 1964, Extraterrestrial particles in Jour. Paleontology, v. 29, no. 6, p. 927-940. 11 sciences: I'alcozoic salts: New York Acad. Sci. Annals, Tyrrcll, W. W., Jr., 1969, Criteria useful in inter- i: Kansas v. 119, p. IGG-185. preting environments of unlike but time- 1'. 68-72. -1966, Abundance of magnetic sl~herulcsin equivalent carbonate units (Tansill-Capitan- \V., 1960, Sll(~ria~~a110 I'crrr~ian s.ilt S~III~~CS:[art11 2nd larnar), Capita11 Reef Complex, west Texas ic 'l'otlilto I'lanctary Sci. Letters, v. 1, p. 325-329. ant1 New Mexrco, in Depositional environ- oc. I'etro- Newell, N. D., Rigby, 1. K., Fischer, A. G., men ts of carbonate rocks: Soc. Econ. l'aleontol- j2. Whiteman, A. J.. Hickox, J. E., and Bradley, ogists and Mineralogists Spec. Pub. no. 14, p. ( icol. soc. J. S., 1953, 7'hc Permian rcef complex of the 80-97. Guadalupe Mountains region, l'exas and New Udden, J. A., 1924, Laminated anhydrite in Texas: 11 evaporite Mexico: San Francisco, Freeman and Co., Geol. Soc. America Bull, v. 35, p. 347-354. :\rts and 236 p. Ogniben, Leo, 1955, Inverse graded bedding in primary gypsum of chemical deposition: Jour. Sed. Petrology. v. 25, p. 273-281.

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