Stratigraphy,paleontology, anddepositional systems ofthe EoceneGub Mountain Formation, Lincoln County, New Mexico- a preliminaryreport by SpencerG. Lucas,New Mexico Museum of NaturalHistory, P. 0. Box7010, Albuquerque, New Mexico 87194; StevenM. CatherNewMexico Bureau of Minesand Mineral Resources, Socorro, New Mexico 87801; PaulSealey New Mexico Museum ol NaturalHistory, P. 0. Box7010, Albuquerque, New Mexico 87194; andJ.Howard Hutchison Museum of Paleontology,University of Calilornia, Berkeley, California 94720

Introduction Bodine (1956) first used the name to refer to "Laramide" shata that lie above the coal-bearingMesa- verde and below the volcaniclasticand volcanic rocks of the Sierra Blanca basin in --l' western Lincoln County, New Mexico (Fig. o v '-srERRA 1). Although it was then clear that the age ( of the Cub Mountain Formation must be Late Bhtf"'o Cretaceousand/or early Tertiary, no precise .4" age data were available.This resulted in var- ied age assignments and differing interpre- tations of the stratigraphic relationships of the Cub Mountain Formation to nearby "Lar- amide" units. Furthermore, no precise in- formation on the depositionalenvironments, provenance, and evolution of the Cub Mountain depositional basin has been pub- Iished. In this paper we present a prelimi- nary effort to determine the stratigraphy,age, depositional environments, and provenance of the Cub Mountain Formation near its type section. o4 .l',.,.:. Intrusivestocks, plugs,and Previous studies sills (dikes not depicted) Ptior to L956,strata of the Cub Mountain Outcroos of Formation either were included in the Upper Cub MountainFormation CretaceousMesaverde Group or apparently were not recognized(e.9., CampbelI, L907; 20 miles Wegemann, 1914; Sidwell, 1946;Allen and fones, 1951).Bodine (1956,p.8) introduced 20 km the term Cub Mountain Formation and mapped its distribution in the vicinity of Capitan. Although he indicated that the for- mation name was for Cub Mountain south of. Carraozo, Bodine did not designate or describea type section for the Cub Mountain FIGURE 1-Outcrops of the Cub Mountain Formation and intrusive igneous rocks in lty of Sierra Formation. (A footnote inadvertently omit- "icit (modified from Dane and Bachman, 1965). ted from Bodine's article would have cred- Blanca basin ited the concept of the Cub Mountain Formation to R. H. Weberand explained that proper definition of the unit was forthcom- Tertiary" age. Lochman-Balk Q96a, p. 58) quartzite, silicic volcanic rocks, chert, gran- ing in an article by Weber.) Nevertheless, listed a "latest Upper (?)(sic) - ite, and petrified wood. He also noted vol- Bodine (L956,p.9) presentedevidence that (?)"age for the Cub Mountain For- canic debris in the upper part of the Cub at least 100 m of strata are missing between mation, and Kelley and Thompson (19(4, p. Mountain Formation and suggestedit might the Cub Mountain Formation and underly- 120)equated the Cub Mountain and McRae provide a basis for dividing the Cub Moun- ing MesaverdeGroup. Although he noted formations (also see Thompson, l9U, 1966, tain into two members, a lower, nonvolcanic that the Cub Mountain Formation could be 1972) and assigned them a "Laramian and member and an upper, volcanic member. as old as Late Cretaceousor as young as "age. Weber (1954,p.106) very tentativelycorre- Miocene,Bodine (1955, p. 10)concluded that Weber Q96a, p. 105)designated and de- lated the Cub Mountain with the EoceneBaca "apparently, the Cub Mountain formation is scribed a type section of the Cub Mountain Formation. another Tertiary intermountain deposit, sim- Formation in SandersCanyon between Cub In the two decadesthat followed Weber's ilar to the Bacaformation of SocorroCounty, and Chaves Mountains (Fig. 2), from the (1964)article, very little work was done on the Galisteo formation of north-central New SW1/6W1/a,sec. L6 to the SW1/+SW1/+,sec. the Cub Mountain Formation. Thompson Mexico, and possibly the McRae formation 24, T9S, R10E. According to Weber 09e), (1966,p.17-19) argaed on a lithologic basis of south-centralNew Mexico."Griswold(1959, the Cub Mountain type section is about 730 for identity of the Cub Mountain Formation p. 12) noted the similarity of the Cub Moun- m of light-colored arkosic sandstone inter- and the McRae Formation in the Elephant tain Formation to the BacaFormation of west- bedded with dominantly red mudrock and Butte area of SierraCounty. He also -unpf9 central New Metco and assignedit an "early minor conglomerateconsisting of pebblesof

New Metico Ceology February 7989 RlOE FIGURE 2-Location of localities, measured stratigraphic section and cub Mountain- contact in the Chavez Canyon-Little cub contact bolwoen Moaav6rd€ Gaoup (lo N) dnd YBU'"u Cub Mountaln .m€aaurod of the "McRae Formation" Formillon (to S) \ .gctlon the distribution '\'1- 4 J in the Sierra Blanca-Cub Mountain area NM local r 344

T Kottlowski (1981,p. 22) indicated a Creta- o J ceous-Paleoceneage. Smith et al. (1985)as- S signed a middle Eocene-earlyOligocene age

M€!av€rd€ Grouo to the Cub Mountain Formation. // (o w, .nd / Cub Mounlaln \ Formailon(to E) I StratigraPhYand dePositional \)\ environments i\ 16 of \----j,1 We examined two stratigraphic sections (7,\-' the Cub Mountain Formation,one partial and one complete,during fune, L987.The,partial section is located on the northern flank of Little Cub Mountain (Fig. 3A); the complete ,K: FIGURE 3-Some outcrop photographs of the Cub Mountain Formation' A, / MOUNTATN Overview of section on-norther-n flank of Little Cub Mountain' B, Basal / (-\ conglomerate of Cub Mountain Formation near Little Cub Mountain (Unit 5 of rieasured section in Figure 4). C, Interbedded sandstone and mudstone at the stratigraphic level of vertebrate-fossil occurrences at NM localities 1384, N 1385 and 1586 (sandstone outcroP is about 5 m thick). D, Root traces and I burrows in red mudstone exposed in Chaves Canyon.

February 1989 New Merico Ceology section is exposedalong Chavesand Sanders Canyons (Fig. 2). At both sections,the Cub Mountain Formation disconformably over- lies strata of the Upper Cretaceous Mesa- verde Group. Although no angular unconformity is apparent locally, Kelley and Thompson (1964)and Kelley (1971)noted that the Cub Mountain Formation overstepspro- gressivelyolder Cretaceousunits to the east. The basal contact is exposedin Chaves Can- yon in the SW'/4,sec. 16, T9S, R10E and north of Little Cub Mountain in the NEl/+,sec. 11, T9S, R10E (Fig. 2). A basal conglomeratic sandstone (Fig. 38) marks the upsection changefrom drabmudstone, sandstone, and Eocene ,NM rare pebbly sandstone of the Mesaverde localities 1384. 1385, and 1386 Group to the coarsersandstone, variegated red mudstone,and conqlomerateof the Cub Mountain Formation(Fig. a). No precise lithologic definition of the Cub Mountain Formation has been published. Perhaps because of ambiguities in its defi- nition, Arkell (1983,1986) extended the term Cub Mountain to include beds mapped as MesaverdeGroup by Weber (1964)and Thompson (1966). Our work supports as- signment of these beds to the Mesaverde Group becauseof their lithologic similarity to Mesaverdeexposures to the west and their dissimilarity to the coarser grained, more brightly hued beds that overliethem, In our view, Arkell's (1983)basal unit and lower part of the main body of the Cub Mountain For- mation are correlative with the Mesaverde Group and are separatedfrom superjacent Tertiary strata by an unconformity. The Cub Mountain Formationis about 730 m thick (Weber, 1964), although the upper part of the sectionin SandersCanyon may be repeated by faulting. Estimated averaBe .g 6c conglomerate:sandstone:mudstoneratio is :.9 about 5:70:25in exposuresnear Cub Moun- =P tain, and the unit becomesfiner grainedup- 6E section. Sandstoneis the dominant lithology >E T ^o I 5 meters and mainly occurs as gray to pink tabular :rr t units that contain abundant horizontal and o low-angle stratification and minor trough crossbedding(Fig. 3C). Conglomerateis largely restricted to the lower one-third of conolomerate/ the formation and commonly occurs in scours conllomeratic ss in the basalportions of sandstoneunits (Fig. trough-crossbedded 38). Pebbles are dominantly chert and sandstone quartzite with subordinant felsic volcanic, planar-crossbedded sandstone, siltstone, Iimestone and silicified sandstone wood clasts.Maximum clastsize is about 10 cm. Mudstone units are tabular in shapeand massive sandstone typically display variegated red coloration. Evidence of bioturbation in mudstones is bioturbated common (Fig. 3D), and calcareousnodules sandstone of probablepedogenic origin were occasion- unconformity ally noted. shale/mudstone Stratification styles in the sandstone lith- osomeare similar to thosedescribed by McKee ironstone et al. (1975) for modern flood deposits of Mesaverde concretions ephemeral Bijou Creek, Colorado. Inter- Group bedded mudstonespresumably accumulated siltstone in vegetatedflood basinsand pondsadjacent to aggrading channel complexes.Overall, fa- ciescharacteristics are quite similar to those FIGURE 4-Measured stratigraphic section of the lower part of the Cub Mountain Formation on the of distal-fan deposits of the EoceneBaca For- northern slope of Little Cub Mountain. SeeFigure 2 for location of section and Table 1 for description mation (Cather and Johnson, 7984,1986), aI- of lithologic units. 13

New Mexico Geology February 7989 though the Cub Mountain Formationcontains which only produced unidentifiable bone scale is inflated ventrally. The free edge of significantly more mudstone. fragments, is in similar mudstone on the the posterior peripheral fragment is bluntly The upper contact of the Cub Mountain southwestern flank of Cub Mountain about acute. The fine texfure of the extemal bone Formation is defined by the first upsection 3 km southwestof the other localities. surfaces,where undamaged, is smooth. occurrence of abundant volcaniclasticdetri- Four identifiable vertebrate fossils, of un- Only two species of Baptemysare recog- tus. Although poorly exposed in Sanders questionable Eocene age, were collected at nized here as valid: Baptemysgarmanii (Cope, Canyon and its tributaries, the contact ap- these localities. Three of these are turtles. 1872) (:Baptemys tricarinataHay, 1908,and pears to be conformable, with interbedding NMMNH (New Mexico Museum of Natural Dermatanyscostilntus Cope, 1872) and Bap- of volcanic and nonvolcanic sandstone and History) P-3501 from locality 1385 consists temyswyomingensis Leidy, 1870 (:8. fluain- mudstone occurring over a stratigraphic in- of ventral fragments of the right third and tilis Hay, 1908).The two taxa are distinguished terval of at leastseveral tens of meters. fourth peripherals articulated with a frag- on the basis of size, omamentation of the ment of the hyoplashal buttress, the distal carapace (carinae), and expansion of the part of a posteriorperipheral, and four costal plastral lobes and bridges. Although the Cub Paleontology and correlation fragments. NMMNH P-j602 from locality Mountain fragments arefully consistentwith We collected fossil bone from the Cub 1385 is a fragment of the medial part of a assignment to the genus Baptemys,they are Mountain Formation at four localities (Fig- hypoplastron and a peripheral 7 fragment. not clearly diagnostic at the species level. 2): 1) NM locality 1384 in the NE1/6EV+ Both of these specimenspertain to Baptemys Size approximates that of large B. garmanii. NEr/aNEtLNEl/r, sec."l.l,T9S, R10E; 2) NM sP. In Wyoming, where the best samples are locality 1385 in the NE1/4SEI/+NEr/+NWI/+ Two of the costal fragments exhibit ripple- known, there is a general increase in size NEl/a,sec. LL,T9S, R10E;3) NM locality1385 like omamentation,and one of them is crossed through time. The Cub Mountain material in the SWr/4SWr/4NEr/4NWr/*NEr/+,sec. 11, by the sinusoidal tract of a pleural sulcus. agrees well in s2e with that of B. garmanii T9S, R10E;and 4) NM Iocality 1387in the The fragment of plastron and the associated and an undescribed taxon from the Cathe- NW1/+SW1/+NW1/4NEI/4NW1/a,s€c. 15, T9S, peripherals (Fig. 5A) are tightly articulated dral Bluffs Member of the Wasatch Forma- R10E.NM localities1384, 1385 and 1386are with the hyoplashal buttress extending onto tion of Wyoming that is intermediate in within about 0.5 km of strike in the same the third peripheral.The marginal4-5 sulcus morphology berweenB. garmaniiand B. uryo- interval of grayish-redmudstone, 94-98 m is finely incised and irregular. The axillary mingensis.The sculpture of the shell agrees above the base of the Cub Mountain For- scale extends just lateral to the peripheral- best with that of the intermediate taxon. The mation (Fig. a; Table 1). NM locality 1387, plastral sufure, and the area covered by the genus Baptemqsis presently known to range

TABLE 1-Measuted stratigraphicsection of part of the MesaverdeGroup and Cub Mountain Forrnationnorth of Little Cub Mountain in the E'l: NEf/+ NWli+NEt/r, sec.f 1, T9S,R10E, and the SEI/+SE1/ISW1l+SEll+,sec.2, T9S,R10E, Lincoln County.Strata dip about 15'to south-southeast.Colors are those of Goddard et al. (1948).Section measured by S. G. Lucasand P. Sealeyduring June 1987using Brinton compassand 1.5-m staff.

Thickness Thickness Unit Lithology (rn) Unit Lithology (m) Cub Mountain Formation(Eocene) 8 Covered. Lower 0.9 m is sandstonelike unit 7. 3.0 20 Sandstone,same color and lithology as unit 18. not measured 7 Sandstone, pale yellowish-orange (10 YR 8/6) and 79 Mudstone, grayish-red (10 R 412),slightly calcareous. grayish-orange (10 YR 714), weathers pale-brown Fossils (NM localities 1384, 1385,and 1386)occur in (5 YR 5/2), quartzose, fine-grained, poorly sorted, lower 3.3 m, upper 18m much coveredby colluvium. 24.4 subrounded, hematitic, slightly calcareous, trough 18 Sandstone, pale-red (70 R 612),weathers to grayish- crossbedded;some carbonaceousmaterial on beds. 18.3 red (10R 4/2),quartzose, medium-grained, well-sorted, Sandstone,pale yellowish-orange(10 YR 8/6)and dark subrounded to rounded, hematitic. Multiple scour yellowish-orange (10 YR 6/6), weathers pale yellow- surfaces divide beds with low-angle, large-scale,ar- ish-brown (10YR 6/2), quartzose,medium- to coarse- cuate crossbedsand planar beds with a thin (0.3 m) grained, moderately sorted, subangular to sub- lenticular (-3 m of strike) bed of limestone pebble rounded, noncalcareous,hematitic; planar crossbeds, conglomeratelike unit 11 in midd.le. 7.6 some thin (3 cm) gravel beds,scoui surfaces. t7 Sandy mudstone, variegated grayish-red (5 R 2/4 and Conglomerate and sandstone. Conglomerateis clast n R 4/4, medium light gray (N 6), light bluish-gray supported;clasts are dominantlyquartzite pebbles as (5 B 5/1), calcareous;much covered by colluvium. 12.8 much as 12 cm in diameter (minor chert and felsic 76 Sandstone,very pale orange(10 YR 8/2),quartzose, volcanics).Sandstone is samelithology as unitT , gray- fine to very coarsegrained, poorly sorted, rounded, ish-orange (10 YR 714), weathers moderate-brown noncalcareous;trough crossbeds. t2.2 (5 YR a/a); clasts are dark yellowish orange (10 YR IJ Shale, light olive-gray (5y 6lI), weathers olive-gray 616),\ght gray (N 8) medium light gray (N 6) and (5 Y 411),noncalcareous, much covered; some mud- medium gray (N 5). 4.0 stonelike unit 19. 3.0 disconformitv Sandstone,grayish orange-pink (5 YR 7 l2), weathers Mesaierde Croup (IJpper Cretaceous) to pale-brown (5 YR 5/2), quartzose, fine-grained, well- Siltstone, light greenish-gray(5 GY 8/1 and 5 G 8/1), sorted, subrounded to rounded, hematitic, noncal- noncalcareous;some ironstone concretions like unit careous;platey weathering of beds. 0.6 z. 13 Mudstone, grayish-red (10 R 4/2), noncalcareous. 3.6 Sandstone, pale yellowish-orange (10 YR 8/6) and t2 Sandstone, same color and lithology as unit 10. o-/ grayish-orange(l0YR7/4), quartzose,fine- to coarse- 11 Conglomerate:matrix is pale yellowish orange (10YR grained, poorly sorted rounded, hematitic, noncal- 8/6); clasts are light gray (N 6), matrtx supported. careous, massive, friable. Maximum clast size is about 1 cm. Clasts are lime- Shale, medium light gray (N 6), weathers yellowish- stone, siltstone, and cherf matrix is quartzose, fine- gray (5 Y 8/1), noncalcareous;contains ironstone con- to medium-grained, poorly sorted, subangularto sub- cretions that are moderate brown (5 YR 3/4), dusky rounded sandstone,slightly calcareous,massive. 0.9 yellowish brown (10 YR UZ), noncalcareous. 10 Sandstone, white (N 9) and very light gray (N 8), Sandstone,very light gray (N 8), weathersmoderate- quartzose,medium- to coarse-grained,poorly sorted, brown (5 yR Aq, quartzose, noncalcareous,biotur- subrounded, noncalcareous,hematitic, massive. 6.1 bated- Covered. 9.1

February 7989 Neu Mexico Geology from the late Graybullian through Bridgerian 1cm (Hutchison, 7980).Baptemys garmanii is known from the later Graybullian through Lostca- binian, the intermediate taxon from earliest Bridgerian (Bridger A and Cathedral Bluffs Member of the Wasatch Formation), and B. wyomingensisfrom middle to late Bridgerian (Bridger B-E). NMMNH P-3603from locality 1385is frag- ments of peripherals (6), costals(2), epiplas- tra (3) and other bones (8) of a turtle we identify as Echmatemyssp. The epiplastral fragments (Fig. 58, C) have extensiveoverlap of the gular scales medially on the dorsal surface. Thickened lateral gular projections enclose a depressed hough medially on the dorsal side, but this trough is not reflected ventrally. The hypoplastral fragments show that the humeral-pectoral sulcus lies poste- rior to the entoplastron, and that there is a thick and nonkinetic sufure between the hyo- and hypoplashon. Other fragmentsshow that the plastral buttressesrise vertically from the plastron and are set medial to the margins of the plastral lobes (Fig. 5D). The pleural- marginal sulcus lies above the proximal su- FIGURE S-Fossil turtles from the Cub Mountain Formation. A, Baptemyssp., NMMNH PJ501, ventral and dorsal views of part ventral view ture of peripheral 11. The plastral of right axillary region comparedto of plastron of B. uryomingensis. scales YD,Echmatemyssp., NMMNH P-3602, 3603, dorsal views of right and left epiplastral fragments (8, overlap extensivelythe dorsal margins of the C) and left hypoplastral fragment (D) compared to a dorsal view of a late WasatchianEchmatemys from plastral lobes. The single proximal fragment Wyoming. Scaleline refers only to Cub Mountain specrmens. of either costal 3 or 5 indicates the presence of an octagonal neural in the neural series and lacks any indication of swelling at the pleural-vertebral margin. The fragments in- dicate a plastral length of as much as ap- proximately 23 cm. The broad plastra with thickened gular of w-$aped ectoloph projections, extensiveoverlap of the plastral scalesdorsally, especiallyon the medial part of the epiplastron, post-entoplastralposition of the humeral-pectoral sulcus, vertical and medial position of the plashal buttresses,and dorsal position of the posteriormost mar- lingual cusp ginal scalesare consistentwith or diagnostic of the common Eocene batagurid Echmate- mys. The systematics of the species within this genus are in need of extensiverevision. The Bridgerian speciesare clearly over split. In the Wyoming sectionswhere the genus is most extensivelyknown and abundant, there is a general increase in size through time. The Cub Mountain material appearsto lie in the size range of later Wasatchian to earliest FIGURE 6-NMMNH P-3604,fragments of brontothere(?)molars from the Cub Mountain Formation. Bridgerian Echmatemysin the Wyoming sec- A, occlusal view of upper molar fragment preserving part of w-shaped ectoloph and a lingual cusp tions. The Wasatchian species from Wyo- B, lateralview of lower molar(?)cuspid fragment. ming, moreover, are characterized by a swelling of the costalbones just lateral to the vertebral-pleural sulcus that is lacking from the Bridgerian and Uintan species(as in the Cub Mountain taxon). This swelling, how- bination of charactersin the Cub Mountain ilarity is to upper molars of Palaeosyopsand, ever, may be absent or only weakly devel- Echmatemysin comparison with the standard Manteoceras(sensu Osborn, L929) grad,e oped in the SanfoseFormation E. ktiiertebralis sequencein Wyoming and Utah indicates a brontotheres. Theseare Bridgerian taxa, and (Cope,1875). The posteriorplacement of the late Wasatchianor earliest Bridgerian age. a brontothere of similar grade is known from humeral-pectoral sulcus is generally typical NMMNH P-3ffi4 is two fragments of a the Baca Formation in the Carthage area of of the Wasatchian species, whereas it typi- mammalian upper cheek tooth from locality SocorroCounty (Lucaset al., 1982). cally overlaps the entire plastron of the 1384 (Fig. 6). These fragments represent a Thus, the fossil evidence from the Cub Bridgerian species.In speciesfrom the Ca- bunolophodont tooth with at least one low, Mountain Formation indicates, without thedral Bluffs Member of the Wasatch For- blunt lingual cusp and a shallow w-shaped question, an Eoceneage. More precisely, a mation, however, the modal condition ectoloph labially. The minimum width of this latest Wasatchian or early Bridgerian age, resembles that of the Wasatchian species. tooth is 20 mm, and parts of its enamel are about 50 +- 2Ma, is probably indicated. This Echmntemasin North America is character- finely lineated. Clearly, this is the tooth of a age is consistent with radiometric-ag" d* istic of arid limited to the Eocene.The com- relatively large mammal. Overall closestsim-

New Mexico Geology February 7989 on dikes and dike swarms that post-dateCub Sands Missile Range, in the critical western Mountain deposition.Moore and Foord (1986, part of the basin. p. 31) recently reported ICAr age-determi- nations of 47.7 + 2.9 Ma provided by R. F. SummarY Marvin of the U.S. GeologicalSurvey on al- Near its type locality, the Cub Mountain kali-gabbro and monzo-gabbro dikes and dike Formation is as much as 730 m of inter- swaflns in the Sierra Blanca vicinitv. bedded sandstone, mudstone, and minor conglomeratethat were deposited by north- east-flowing braided streams. Fossil verte- Paleocurrentsand provenance brates collected about 100 m above the base indicate an Eoceneage (nearthe Wasatchian- Paleoflow during deposition of the Cub -r Mountain Formation, as shown by pebble Bridgerian boundary, about 50 2 Ma). imbrication and parting-step lineation, was Lithologic and paleocurrent data for the Cub northeasterly in the study area (Fig. 7). Be- Mountain Formation suggestderivation from causethe study areais locatedin the western source terranes to the southwest that ex- partof the SierraBlanca basin, paleoflowwas posed dominantly older sedimentary rocks. roughly tangential to the present basin mar- Potential source regions include the Lar- gin. These data indicate that Eocenedrain- amide Rio Grande and Tularosa uplifts al- age in the Sierra Blanca basin was not though further study is needed to better centripetal, which supports the concept that constrain the provenance of the Cub Moun- on synclinal downwarping of the basin postdated FIGURE7-Paleocurrent-rose diagram based tain Formation. 20 rneasurementsof pebbleimbrication and parF AcxNowr-EoctrcNrs-We thank the own- deposition of the Cub Mountain Formation For- ing-steplineation from the Cub Mountain ers of the StephensonRanch, Inc. for access (Kelley and Thompson, 1964;Kelley, l97l). Cub Mountain * ChavesCanyon-Little and C. E. Chapin Most detrital components of Cub Moun- I::"" to Cub Mountain outcrops tain sandstonesand conglomerateswere de- and R. M. Chamberlin for assistancein the rived from older sedimentary sources. field. We benefited from reviews by R. M. Quartzite, chert, and subordinant felsic vol- An altemative source region for the Cub Chamberlin, C. E. Chapin, E. H. Lindsay, canic pebblesdominate conglomeratesin the Mountain Formation is the Tularosa uplift W. R. Seager,and R. H. Weber. The A. M. study area;pebbles of theselithologies occur (Fig. 8; Herrick, L9M, p. 75; Eardley, 1962, Alexander endowment of the University of in trace amounts in the underlying Mesa- p.399; Kottlowski et al., 1955,p. 73;Chapin California Museum of Paleontology funded verde Group and are common in conglom- and Cather, 798L),a poorly documented and the artwork in Figure 5, and R. Pencedrew erate beds of the Ash Canyon Member of the controversial uplift that may have collapsed the artwork for Figure 6. Crevasse Canyon Formation (Wallin, 1983) to form the present TularosaBasin. With the to the southwest. Other pebble varieties exception of Mesozoic units penetrated by References (limestone, sandstone, siltstone, silicified three wells in the exheme northeastern part Allen, J. E., and Jones,S. M., 1951,Capitan-Canizozo- wood) in the Cub Mountain Formation were of the TularosaBasin near Three Rivers (King Chupadera Mesa region: Roswell Geological Society, clearly derived from Mesozoicand Paleozoic and and data Guidebook to 5th Field Conference,12 pp. Harder, 1985),borehole outcrop Allen, J. E., md Kotdowski, F. E., 1981,Roswell-Ruidoso- sedimentary units. Although Weber (1964) indicate poorly consolidated Quaternary to Valley of Fires: Socono, New Mexico Bureau of Mines reports minor granitic clasts in the Cub Tertiary(?) sediments directly overlie Per- and Mineral Resources,Scenic Trip 3, 3rd edition, 96 Mountain Formation, none were noted dur- mian strata throughout the eastem part of PP. Arkell, B. W., 1983, Geology and coal resourcesof the ing the present study. the basin. Where absent, Mesozoicsedimen- Cub Mountain area, Siena Blancacoal field, New Mex- Preliminary petrographic analysisof three tary units may have been stripped during ico: unpublished M.S. thesis, New Mexico Institute of sandstones indicates a dominance of sedi- broad upwarping, possibly during the Late Mining and Technology, Socono, 104 pp. mentary rock fragments in the lithic fraction. Cretaceous or early Tertiary. Alternatively, Arkell, B. W., 1986,Stratigraphy of western part of Siena Blanca in Ahlen, Hanson,M. andZidek, Contributions from crystallinebasement rocks these units may have eroded basin; J. L., 8., been during J. (eds.), SouthwestSection ofAAPG Transactionsand appear to be minimal. Minor but persistent late Tertiary crustal extension (W. R. Seagea Guidebook of 1986Convention. Ruidoso.New Mexico: amounts of volcanic rock fragments, plagio- oral comm. 1988).At present, the Tertiary New Mexico Bureau of Mines and Mineral Resources, clase,and biotite are present throughout the structural development of the TularosaBasin pp.73-75. Bodine, M. W., Jr.,7956,Geology of the Capitancoal field, Cub Mountain Formation. However, as noted area is poorly understood, primarily due to Lincoln County, New Mexico: New Mexico Bureau of above, this material may have been recvcled lack of borehole and seismicdata on the \A/hite Mines and Mineral Resources,Circular 35,27 pp. from the underlying Mesaverde Gioup. Campbell, M. R.,1907,Coal in the vicinity of Fort Stanton Provenanceof the Cub Mountain Formation reseruation, Lincoln County, New Mexico: U.S. Geo- thus can be only loosely constrainedat pres- logical Suruey, Bulletin 315, pp. 431.-4U. Cather, S. M., and Johnson,B. D., 1984,Eocene tectonics en! source terranes were to the southwest and depositional setting of west-centralNew Mexico and consisted primarily of older sedimen- and eastemArizona: New Mexico Bureauof Mines and S;e,,o Blonco /y'..,i Mineral Resources,Circular 792,33 pp. tary rocks. At least two potential source re- bosrn t. \tr:r;t:i/\- Cather, S. M., and B. C., f986, Eocenedepo- ,p,'o^ i Johnson, gions can be postulated. \ I I sitional systemsand tectonicframework of west-central r"to^ \ I I The Rio Grande uplift (Fig. 8) of Seager New Mexico and eastem Araona; lz Peterson, J. A. and Mack (1986)was a northwest-trending, *l-\ (ed.), Paleotectonicsand sedimentation in the Rocky / \- late Laramide uplift in south-central New x,> Tuloroso Mountain region, United States:American Association { uplift Mexico that shed clasticdetritus (Love Ranch -.t------J of Petroleum Geologists,Memoir 41, pp,623-552- -\ Chapin, C. E., and Cather, S. M., 1981,Eocene tectonics Formation) mostly during Eocenetime. Sed- +{.- and sedimentation in the Colorado Plateau-Rocky iments were transported both to the south- L__i Mountain area: Arizona Geological Society Digest, v west into the Potrillo basin and northeast 74, pp. 1.73-798. into the Love Ranch basin. / ou",on" Dane, C. H., and Bachman,G. O., 1965,Geologic map Deposits of the poleoflow of New Mexico: U.S. GeologicalSurvey, 2 sheets,scale Love Ranchbasin becomemarkedly finer to- 1:500,000. ward the northeast, in the direction of the Eardley,A. J., 1962,Structural geologyof North America: Harper New York, 2nd edition, 743 pp. Sierra Blanca basin. Clast types are locally FIGURE gl,".urnia" paleogeographicmap and Row, Goddard,E. N., Trask,P D., DeFord,R. K., Rove,O. N., variableand include Mesozoic,Paleozoic, and showing Sierra Blancabasin, averagepaleoflow in Singewald,J. T., and Overbeck,R. M., 1948.Rock-color Precambrianlithologies (Seager,L981; Seager the study area, and postulated sourceareas for the chart: GeologicalSociety of America, Boulder. and Mack, 1985). Cub Mountain Formation. Griswold, G. 8., 1959,Mneral deposits of Lincoln County,

February 1989 Nru MexicoGeology New Mexico:New Mexico Bureauof Mines and Mineral Resources,Bulletin 57, 117 pp. NewMerico Geological Society FrankWayne Gampbell Herrick, C. L., 1904,Lake Otero, an ancientsalt lake basin SpringMeeting in southeasternNew Mexico: The American Geologist, (1s47-1988) u. 34, pp. 174-189. The New Mexico GeologicalSociety will Hutchison, J. H., 1980, Turtle stratigraphy of the Will- wood Formation, Wyorning-preliminary results: Uni- hold its annual spring meeting on Friday, versity of Michigan, Museum of Paleontology,Papers April 7, 1988 in Macey Center at the New Frank W. Campbell was born on May 31, on Paleontology27, pp. 175-77E. 1947 in Long Beach, California, the son of Kelley, V C.,1977, Geology of the Pecoscountrt south- Mexico Institute of Mining and Technology, eastemNew Mexico: New Mexico Bureauof Mines and Socorro, New Mexico. This meeting pro- Paul and Zella Campbell. He came to New Mineral Resources,Memoir 24, 78 pp. motes the disseminationof the resultsof re- Mexico Institute of Mining and Technology Kelley, V C., and Thornpson, T. 8., 1954,Tectonics and general geology of Ruidoso-Carrizozo region, central cent researchon the geologyof New Mexico. to study geology and graduatedwith a BS New Mexico: New Mexico Geological Society, Guide- The morning sessionscover geophysics/ degreein1971, the sameyear he marriedSue book to 15th Field Conference,pp. 1.1.0-727. petrology/structuralgeology and stratigra- Lynn Rose.They moved to RapidCity, South King, W. E., and Harder, V M., 1985,Oil and gas poten- tial of the TularosaBasin-Otero platfom-Salt Basingra- phy/sedimentologyipaleontology.The after- Dakota where Frank attended the South ben area, New Mexico and Texas:New Mexico Bureau noon sessionscover geochemistry/economic Dakota Schoolof Mines. He receivedan MS of Mines and Mineral Resources,Circular 198,36 pp. in geologythere in 1975. openings Kottlowski, F E., Flower, R. H., Thompson, M. L., and geologyand hydrology/environmentalgeol- degree Job Foster, R. W., 79fi, Stratigraphic studies of the San ogy.Registration materials are available from in geologywere scarceat that time, so Frank Andres Mountains, New Mexico: New Mexico Bureau Virginia T. Mclemore, New Mexico Bureau and Suemoved back to California,where he of Mines and Mineral Resources,Memoir 1, 132pp. Lochrnan-Balk, C., 1964,Lexicon of stratigraphic names of Mines and Mineral Resources,Socorro, operated a pet shop and indulged his love used in Lincoln County, New Meico: New Mexico New Mexico 87801,(505) 835-5521. of tropical fish. Geological Sooety, Guidebook to 15th Field Confer- In 1978,when there was an increasedin- ence,pp. 57-61. Lucas,S. G., and Ingersoll,R. V, 1981,Cenozoic conti- FallField Conference terestin coal in New Mexico,the New Mex- nental deDositsof New Mexico-an overview: Geoloq- ico Bureau of Mines and Mineral Resources ical Sociei of America, Bulletin, Part I, v. 92, pp. 91/- The New Mexico Geological Society will (NMBMMR) had three openings for coal 932. Lucas,S. G., Wolberg,D. L., Hunt, A., and fthoch, R. M., hold its 40th annual field conference in the geologists.Frank applied, along with many 1982,A middle Eocenetitanothere from the BacaFor- Acoma-Grants-Zuni-Gallup area of west- others, and was hired to fill one of these mation, southtentral New Mexico: Journal of Paleon- central New Mexico from September 29 to tology, v 56, pp.542-!45. positions.His projectsincluded the mapping McKee,E. D., Crosby,E. J., and Benyhil,H. L.,Jr.,1967, October 1, 1989. Several stops on this bus and stratigraphicinterpretation of coal out- Flood deposits, Bilou Creek, Colorado,June L955:Jour- tour will emphasize the southeastern Colo- crops in the FenceLake-Salt Lake coal field; SedimentaryPetrology, v.37, nal of pp.839-851. rado Plateau tectonic transition Moore, S. L., and Foord, E. E., 1986,Roadlog from Inn as a zone of he set up and directedthe drilling program of the Mountain Gods to the RuidosoSkiArea on Siena where Laramide strike-slip faults and mon- in this field. Frank has been one of the prin- BlancaPeak; in Ahlen, J. L., Hanson, M. E., and Zidek, oclinal uplifts have partially collapsed in re- cipal investigators in the NMBMMR's four- J. (eds.), Southwest section of AAPG Transactionsand Guidebook of 1986Convention, Ruidoso,New Mexico: sponse to late Cenozoic extension and year study of the quality and quantity of New New Mevico Bureau of Mines and Mineral Resources, magmatism. Other stops will address ad- Mexicostrippable coals. PP.29-36. vances in Cretaceous, and Tertiary Osborn, H. F.,7929, The titanotheresof anoent Wyo- furassic, Beginning in the early 1980'sFrank de- ming, Dakota, and Nebraskavolume t: U.S. Geological stratigraphy; the relationship of coals to veloped a coal anaiyticallaboratory at the Suruey, Monograph 55, pp. 1-701. basement structures and shore lines; and the NMBMMR capableof determining heating and Seager,W. R., 1981,Geology of the Organ Mountains recognition zones. Stops southern San Andres Mountains, New Mexico: New of paleoweathering values, proximate and ultimate analyses, Mexico Bureauof Mines and Mineral Resources,Mem- at the scenic Acoma and Zuni Pueblos will forms of sulfur, ash-fusion temperatures, oir 36,97 pp. allow for brief shopping sprees and cultural trace- Seager,W R., and Mack, G. H., 1986,Laramide paleo- water-solublealkalies, maior oxides,and enrichment. The will convene at, tectonics of southern New Mexico; in Peterson, ). A. conference element composition of coals. He was the (ed.), Paleotectonicsand sedimentation in the Rocky and return to Albuquerque, just prior to the first professionalstaff member to routinely Mountain region, Uruted States:American Association AAPG Rocky Mountain Section meeting. For of Petroleum Geologists,Memoir 41, pp. 569-685. use a personal computer for his work. At a Sidwell, R., 19,16,Effects of dikes and displacementmove- additional information contact co-chairmen time when PCswere not in use in the Bureau, ments on sedimentsin Capitan quadrangle,New Mex- Orin Anderson (505/835-5722) or Richard he bought one himself and installedit in his ico:American Mineralogist, v.31, pp. 65-70. Chamberlin (505i835-5310) at the New Mex- Smith, L. N., Lucas,S. G., and Elston,W 8., 1985,Pa- office.Frank's scientific accomplishments are leogene stratigraphy, sedimentation and volcanism of ico Bureau of Mines and Mineral Resources, evident through his many publishedpapers New Mexico; ir Flores,R. M., and Kaplan, S. S. (eds.), Socorro. New Mexico 87801. Cenozoic paleogeographyof the west-central United and open-file reports.At the time of his death Stabes:Denver, Rocky Momtain Section SEPM, pp.293- publication was imminent of GM-62, Ceology 315. and coal resourcesof FenceLake 1:50,000 quad- Thompson, T. 8., 1964,A stratigraphic section of the Siena Blane volcmics in the Nogal Peak area, Lincoln County, rangle, NerrlMexico, a compilation by Frank New Mexico; New Mexico Geological Society,Guide- of eight 1:24,000-scalequadrangles in west- book to 15th Field Conference, pp. 76-77. centralNew Mexico. Thompson, T. 8., 796, Geology of the SierraBlanca, Lin- coln and Otero Counties, New Mexico: Unpublished Frank loved sciencefiction, military his- Ph.D. dissertation,University of New Mexico,Albu- tory, classicalmusic, and opera.But his most querque, 1it6 pp. job Thompson, T. 8., 7972, Siena Blanca igneous complex, important interestaway from his was his New Mexico: GeologicalSociety of America Bulletin, v. family. He adored his wife Sue and their two 83, pp. 2341-2356. children, Elizabeth Katie born in 7975 and Wallin, E. T., 1983,Stratigraphy and paleoenvironments of the Engle coal field, Siena County, New Mexico: Paul Clayton born in 1981. Unpublished M.S. thesis,New MexicoInstitute of Min- Frank Campbell died on December3, 1988. ing and Technology,Socono, 104 pp. Throughout the years and final months of Weber,R. H., 19&, Geologyof the Carrizozoquadrangle, New Mexico: New Mexico Geological Society,Guide- his illnesshe showed us all how to laugh in book to 15th Field Conference,pp. f00-109. spite of pain and how to live in spiteof dying. Wegemann, C. H., 1974,Geology and coal resourcesof the Siena Blancacoal field, Lincoln and Otero Coun- He was a shining example of quiet courage. ties, New Mexico: U.S. GeologicalSutret Bulletin 541, -Iyn pp. 479-542 tr Brandaold

New Mexico Geology February \989 "17