Evidence for a Marine Incursion Along the Lower Colorado River Corridor

CRevolution 2: Origin and Evolution of the Colorado River System II themed issue

Evidence for a marine incursion along the lower Colorado River corridor

Kristin McDougall1 and Adriana Yanet Miranda Martínez2 1Geology, Minerals, Energy, and Geophysics Science Center, U.S. Geological Survey, 2255 N. Gemini Drive, Flagstaff, Arizona 86001, USA 2Posgrado en Ciencias de la Tierra, Instituto de Geología, Universidad Nacional Autónoma de México, México D.F. C.P. 04510, México

ABSTRACT INTRODUCTION be found (~74) and examining new samples collected in the past 15 yr (~100). The Bouse Foraminiferal assemblages in the strati- The depositional setting of the Bouse Forma- foraminiferal faunas were compared to forami- graphically lower part of the Bouse Forma- tion, preserved as a series of basins along the niferal faunas in saline lakes and estuaries. tion in the Blythe basin (lower Colorado lower Colorado River corridor, is controversial In addition, the presence of Charophytes and River corridor, western USA) indicate and is variously attributed to a lacustrine origin reworked microfossils was noted. Arguments marine conditions, whereas assemblages in in a series of lakes, or a marine incursion related supporting the presence of a saline lake were the upper part of the Bouse Formation indi- to the proto–Gulf of California, which affected examined in light of the foraminiferal analysis. cate lacustrine conditions and suggest the the Bouse Formation in the Blythe basin. The Flood deposits, which are cited as evidence of presence of a saline lake. Benthic forami- lacustrine origin suggests deposition of the lake deposition, do not occur or have not been niferal assemblages in the lower part of the Bouse Formation in a series of lakes that fi lled found in the Blythe basin; mapping, sedimen- Bouse Formation are similar to lagoonal and spilled from one basin to the next until sys- tary studies, and structural analysis of the area and inner neritic biofacies of the modern tem was integrated and the Colorado River was are inadequate to consider uplift or the lack of Gulf of California. Evidence suggesting a a through-fl owing river (House et al., 2005a, uplift as a viable means of proving deposition change from marine to lacustrine conditions 2005b, 2008; Spencer et al., 2005, 2008). Argu- in a marine or saline lake environment. Many includes the highest occurrence of planktic ments in favor of a lacustrine origin of the Bouse of these studies are currently ongoing. Isotopic foraminifers at an elevation of 123 m above Formation are based on isotopic analyses (Spen- data are frequently used to advocate a lacus- sea level (asl), the change from low diversity cer and Patchett, 1997; Buising, 1990; Poulson trine origin for the Bouse Formation. Although to monospecifi c foraminiferal assemblages and John, 2003; Roskowski et al., 2010; Spen- the Sr data suggest deposition in a lacustrine composed only of Ammonia beccarii (between cer et al., 2013), step-like maximum elevations environment, the data are limited for the older 110 and 126 m asl), an increase in abundance of the Bouse paleolakes suggesting that no uplift or basal Bouse Formation, and in the interval in of A. beccarii specimens (above ~110 m asl), or southward tilting has occurred since deposi- which marine microfossils and high Sr values increased number of deformed tests (above tion of the unit (Spencer et al., 2008, 2013), and overlap there is evidence of mixing of marine ~123 m asl), fi rst appearance of Chara (at sedimentological evidence of fl oodwater infl ux and river water. The high strontium isotope ~85 m asl), lowest occurrence of reworked derived from northern sources immediately values characteristic of the Bouse Formation Cretaceous coccoliths (at ~110 m), a decrease preceding Bouse Formation deposition in the are considerably higher than modern Colorado in strontium isotopic values (between 70 and Mohave and Cottonwood Valleys (House et al., River values, suggesting that additional study 120 m), and δ18O and δ13C values similar to 2008; Spencer et al., 2013). An alternative inter- is needed to understand the source and concen- seawater (between 70 and 100 m asl). Plank- pretation suggests that the Bouse Formation tration of the strontium before the marine or tic foraminifers indicate a late Miocene age accumulated in lakes along the northern part nonmarine signal can be determined. Carbon between 8.1 and 5.3 Ma for the oldest part of of the lower Colorado River corridor, but in the and oxygen isotopic ratios are also limited and the Bouse Formation in the southern part Blythe basin, the formation was initially depos- the marine or nonmarine interpretation of these of the Blythe basin. Benthic and planktic for- ited in a marine environment at the northern end values is reexamined. aminifers correlate with other late Miocene of the proto–Gulf of California (Buising, 1988, sections in the proto–Gulf of California and 1990). Arguments in favor of the marine origin GEOLOGIC SETTING suggest that the basal Bouse Formation in for the lower part of the Bouse Formation in the the Blythe basin was deposited at the north- Blythe basin are the presence and distribution of The Bouse Formation (Metzger, 1968) ern end of this proto-gulf. After the marine marine fossils. uncon formably overlies a Miocene fanglomer- connection was restricted or eliminated, The purpose of this paper is to document ate and is overlain by the Bullhead alluvium in the Colorado River fl owed into the Blythe the presence of foraminifers in the Bouse the Blythe basin, and is composed of a basal basin, forming a saline lake. This lake sup- Formation of the Blythe basin and determine limestone overlain by silts, clays, sands, and ported a monospecifi c foraminiferal assem- if they existed in a marine, saline lake, or a tufa (Fig. 1). Metzger (1968) designated blage of A. beccarii until the lake spilled into mixed environment. This goal was achieved 233.8 m of sediments penetrated in the U.S. the Salton Trough and the Colorado River by reexamining previously collected micro- Geological Survey test well Mf11684 as the became a through-fl owing river. paleontology slides and residues that could type section for the Bouse Formation (Fig. 2).

Geosphere; October 2014; v. 10; no. 5; p. 842–869; doi:10.1130/GES00975.1; 13 ﬁ gures; 12 tables; 1 plate; 1 supplemental ﬁ le. Received 2 August 2013 ♦ Revision received 14 April 2014 ♦ Accepted 11 July 2014 ♦ Published online 29 August 2014

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PALEONTOLOGY Generalized Stratigraphy Formations or units Early paleontologic studies suggested that Figure 1. Generalized strati- Recent Alluvium the Bouse Formation was deposited in a marine graphic column and ages, based embayment at the northern end of the Gulf of on studies by Buising (1990, California during the latest Miocene to Pliocene. 1993) with the addition of radio- This interpretation is supported by the presence metric ages that constraint Bullhead Alluvium of benthic and planktic foraminifers (Durham the age of the Bouse Forma- and Allison, 1960; Hamilton, 1960; Metzger, tion. No scale is given due to the Lawlor Tuff 4.83 Ma 1968; Smith, 1960, 1969, 1970; Winterer, 1975; variable thickness of the Bouse Buising, 1988, 1990; McDougall, 2008a), as Formation. Dates in the Osborne well as other invertebrates (Metzger, 1968; Wash strata of Buising (1988) Bouse Formation Taylor, 1983; A. Cohen, 2012, personal com- are from Fugro, Inc. (1975, cited mun.) and vertebrates (Crabtree, 1989). Other in Reynolds et al., 1986) and fossils in the Bouse Formation include diatoms, Buising and Beratan (1993). Tbbf = Bouse basin fill ostracodes, coralline algae, barnacles, mollusks, The presence of the Lawlor Tbbm = Bouse basin margin gastropods, crabs, and ﬁ sh (Table 1). The dis- Tuff and the dates for this tuff tribution of these groups is not addressed in are from Reynolds et al. (2008), this paper and needs additional study, as these

Sarna-Wojcicki et al. (2011), tuff age 9.2 + 0.3 Ma groups include marine, brackish, and fresh- and Spencer et al. (2013). basalt age 9.6 + 0.6 Ma water species. Our study focuses primarily on Osborne Wash strata the foraminifers, which are primarily a marine of Buising (1988) group. Nonmarine occurrences of foraminifers are limited and distinctive, and therefore easily recognized. Micropaleontologic samples collected and Two additional reference sections were also the Blythe basin were summarized previously analyzed from various research efforts are designated: (1) outcrops south of Bouse Wash (Metzger et al., 1973; Olmsted et al., 1973; P.J. documented in Tables 2–11. The taxonomy was and east of the Colorado River fl ood plain, Fritts, 1975, unpublished report, provided by evaluated and notes are given in the Supplemen- where 65.5 m is exposed; and (2) outcrops in K. Howard, 2012, personal commun.; Winterer, tal File1. Some of the foraminiferal slides from sections 9 and 16, southeast of Cibola, where 1975; Turak, 2000). The Bouse Formation is outcrops and wells drilled in conjunction with 30.5 m of the basal limestone is exposed identifi ed in the Blythe basin between –173 m the Lower Colorado River Project (LCRP) and (Metzger, 1968). Approximately 46 m of the below sea level (bsl) and 330 m above sea level examined by P.B. Smith (Metzger et al., 1973; reference section south of the Bouse Wash (asl), (Metzger et al., 1973; Buising, 1990; Smith 1970) are available in the U.S. Geologi- was resampled for paleomagnetics and micro- Spencer et al., 2008, 2013). cal Survey Micropaleontologic collection (Flag- fossils (D. Malmon, 2008, personal commun.; The Bouse Formation was tentatively staff, Arizona). Previously unpublished data Malmon et al., 2011). Only spot samples were assigned to the Pliocene based on post-Mio- were added to the checklists. Some of the mate- taken from the reference section southeast of cene fossils in sections near Yuma (Metzger, rial used to generate the published checklists has Cibola, although a section has been recently 1968; Smith, 1970; Metzger et al., 1973). An not been located at the U.S. Geological Survey sampled for microfossils in Hart Mine Wash ash bed stratigraphically located in the upper or at the Arizona Geological Survey (Rauzi, near Cibola (this paper; Fig. 2). part of the Bouse Formation in the southwest 1999) and remains missing. The Bouse Formation was defi ned in the Blythe basin, (near Buzzards Peak) and in the A couple of stratigraphic sections were Blythe basin and its geographic extent has Bristol basin (near the town of Amboy) corre- examined (Bouse Wash, Big Maria Quarry, since been expanded to include the Mohave- lates with the 4.83 Ma Lawlor Tuff (Reynolds and Hart Mine Wash; Fig. 2), but most of the Cottonwood, Chemehuevi, and Bristol basins et al., 2008; Sarna-Wojcicki et al., 2011). A samples available are spot samples and have along and near the lower Colorado River cor- lower age limit for the Bouse Formation in the little stratigraphic information. The units in the ridor in Arizona, California, and Nevada Blythe basin is from the underlying Osborne Bouse Formation are time transgressive, so the (Metzger, 1968; Olmsted, 1972; Mattick et al., Wash strata of Buising (1988, p. 12) in the stratigraphic correlation between sections and 1973; Metzger et al., 1973; Metzger and Loeltz, western Buckskin Mountains. A basalt near the spot samples is diffi cult to infer. In this study 1973; Olmsted et al., 1973; Carr and Dickey, top of the Osborne Wash strata (Buising, 1988) and in previous studies (Spencer et al., 2013), 1980; Buising, 1988; Turak, 2000; House et al., is dated as 9.60 ± 0.60 Ma (Fugro, Inc., 1975, elevation is used as a proxy to identify strati- 2008). Except for a disputed outcrop near the cited in Reynolds et al., 1986; Buising, 1988) graphic position because of the diffi culty in Laguna Diversion and Imperial Dams (sample and a tuff bed from the upper clastic unit (i.e., defi ning stratigraphic position based on lithol- locality J219 of Winterer, 1975; see also Olm- equivalent to Osborne Wash strata of Buising, ogy. Although elevation is not a good proxy, sted et al., 1973, fi g. 15 therein), the Bouse 1988) is 9.2 ± 0.3 Ma (Buising and Beratan, until the amount of faulting and subsidence Formation is identifi ed only in the subsurface 1993). These dates suggest that deposition of in the Yuma area of Arizona (Olmsted et al., the Bouse Formation in the Blythe basin began 1Supplemental File. Taxonomic notes and sample locations. If you are viewing the PDF of this paper 1973; McDougall , 2008a; Spencer et al., 2013). after 9.2 Ma but ceased after ca. 4.83 Ma, when or reading it offl ine, please visit http://dx .doi .org Numerous core holes and wells that encoun- the water breached the paleodam and spilled /10.1130 /GES00975 .S1 or the full-text article on www tered the Bouse Formation in the subsurface of into the next basin. .gsapubs .org to view the Supplemental File.

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116°0′0″W 115°0′0″W 114°0′0″W

Topock Amboy tuff

Bristol Basin

Cadiz Parker Lake Danby Lake Parker Mf11689 Mf11679 ? 34°0′0″N Big Maria Mf11677 Mf11681 34°0′0″N Mtns Bouse Wash Section Mf11684 (type section)

Mf11680 Big Maria Quarry

Blythe Basin Blythe

Mf11676 San Andreas Fault Zone Mf11678

Salton Sea Mf11682 Mf11683

Hart Mine Trigo Mtns Wash Buzzards Peak tuff Chocolate 33°0′0″N 33°0′0″N Explanation 115°0′0″W 114°0′0″W

Topock Postulated paleodam Modern lake / reservoir / dry lake playa

Tuff locality Maximum extent of late Miocene to early Pliocene lakes and the Bouse Fm. MicrofossilMicrofossil locality,locality, outcrooutcropp Gulf of California / Salton Trough Microfossil locality, well CrossCross section Figure 2. Index map of study area showing locations of the Blythe and Bristol basins, microfossil localities, and isotope localities. The Blythe basin includes the area from Parker Dam south to the Chocolate Mountains (Mtns) and is divided into northern (Parker Dam to Big Maria Mountains) and southern (Big Maria Mountains to Chocolate Mountains) subbasins. The Bristol basin includes the area west of Parker (west of LCRP 27 to west of the Amboy tuff locality). Micropaleontologic samples (red dots) include samples from the U.S. Geological Survey Micropaleontology collection (Flagstaff, Arizona) and samples from the literature (Smith, 1970; Winterer, 1975). Isotope samples (green triangles) are from the literature (Spencer and Patchett, 1997; Buising, 1990; Poulson and John, 2003; Roskowski et al., 2010; Spencer et al., 2013). The Amboy and Buzzards Peak tuff localities are shown with red stars. The maximum extent of the late Miocene to Pliocene lakes is indicated. Cross section used in following ﬁ gures is indicated.

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TABLE 1. LIST OF OTHER ORGANISMS FOUND IN THE BOUSE FORMATION AND THEIR ECOLOGY IMPLICATIONS Organisms Environment Chara (Metzger,1968; Metzger et al., 1973; Common inhabitants of shallow, oligotrophic fresh waters; some species can tolerate brackish-water conditions K. McDougall, personal data) with salinities approaching 20 ppt (Olsen, 1944; Wood, 1952; Proctor, 1961; Burne et al., 1980). Coralline algae: Sporolithon, and Corallines live in varying depths of water, ranging from periodically exposed intertidal settings to 270 m water possible Lithothamnion(?) (A. Cohen, depth; some species can tolerate brackish (Aquirre et al., 2000) or hypersaline waters (Thornton et al., 1978); 2012, personal commun.) no freshwater species exist. Ostracodes: Candona, Candoniella, Cyprideis, These ostracodes are both brackish and freshwater types (identifi ed by I.G. Sohn, in Metzger, 1968, p. D133). Cytheromorpha sp., Ilyocypris and Limnocythere (Metzger, 1968; Metzger et al., 1973; Winterer, 1975; Turak, 2000) Barnacles: Balanus subalbidus Van Syoc, 1992 Balanus subalbidus is found in salinities between 0.1 and 16 ppt (Poirrier and Partridge, 1979). (or Balanus canabus of Zullo and Buising, 1989) (Winterer, 1975; Buising, 1988; Turak, 2000) Clams (Bivalvia): Diplodonta, Halodakra, Diplodonta—Marine, continental shelf water depths. Species probably misidentifi ed in Bouse Formation Lucinidae?, Macoma, Pitar?, Mulinia, Veneridae (C. Powell, 2013, personal commun.) (Metzger, 1968; Metzger et al., 1973) Halodakra has been synonymized with Neolepon, which is marine, found at continental shelf water depths. Species probably misidentifi ed in Bouse Formation (C. Powell, 2013, personal commun.). Lucinidae—marine, mostly shallow infaunal in temperate to tropical seas, but some forms contain chemosynthetic bacterial and are found at very deep depths, in excess of 6000 m, worldwide. Macoma—marine, mostly shallow infaunal in cold to tropical seas at water depths from the intertidal zone to bathyal. Mulinia—brackish to marine, shallow water. Veneridae usually in warm and shallow water, but found to the Arctic Ocean, usually in shallow water, but can be found deeper. Gastropods: Batillaria californica, Barleeria?, Batillaria inhabits shallow water in estuarine and marine environments, lives in warm- temperate to tropical waters Fontelicella, Physa, Hydrobiidae?, Pyrgulopsis, of the Caribbean and East Asia (D.W. Taylor, in Metzger, 1968), shallow brackish water in the mud of the and Tryonia? (Metzger, 1968; Metzger et al., intertidal zone (Taylor, 1983). 1973; Taylor, 1983; Spencer and Patchett, 1997) Barleeria—marine, intertidal to shallow subtidal. This genus probably misidentifi ed (C. Powell, 2013, personal commun.). Physa and Pyrgulopsis (=Fontelicella)—freshwater snails (Metzger, 1968; Hershler, 1994; Spencer and Patchett, 1997) Hydrobiidae—Most species of this family live in fresh water (lakes, ponds, rivers, streams), but some are found in brackish water or at the borders between fresh water and brackish water. A few occur in marine environments on sandy or muddy bottoms between algae and sea grass. Tryonia are desert spring snails, all fresh water usually associated with springs. Crabs, small chelae (Taylor, 1983) Marine, fresh water, land. Fish: Colpichthys regis (False Grunion) C. regis nearshore areas of the upper Gulf of California; distribution is discontinuous across the Colorado River (Todd, 1976; Crabtree, 1989) delta (Crabtree, 1989).

noted by Metzger et al. (1973) in the Blythe Benthic foraminiferal diversity in the Bouse (3) nine to fi ve species in the southern part of basin is understood and corrected for, eleva- Formation of the Blythe basin increases from the Blythe basin at 110–123 m asl (Hart Mine tion, at least, allows the samples to be placed north to south and decreases with increased Wash, Mf11682, and Mf11683). in relation to each other. Metzger et al. (1973) elevation (i.e., the younger portion of the Bouse Higher benthic diversities are associated with noted regional downwarping of the Palo Verde Formation) (Fig. 3). Diversity is defi ned here as the presence of planktic foraminifers in the Hart Valley (southern Blythe basin) centered at the the number of species per sample, but since no Mine Wash section (110–113 m, possibly in the city of Blythe, California, and small-scale dis- standardization of sample size or picking tech- sample at 123 m asl) and Mf11680 (~116 m placements near the mountains southeast of niques were used, this should be considered asl). Planktic foraminiferal diversity is low (≤2 Cibola that result in a differential movement the species richness. Geographically, there are species) in most samples. A maximum diversity of 300–600 m. three noticeable breaks in the diversity: (1) in of four species occurs in Mf11676 (sample at Foraminiferal assemblages in the Bouse For- the Chemehuevi, Mohave, and Cottonwood –80 m bsl) and Mf11682 (110 m asl). In the mation consist of up to 16 benthic and 7 planktic basins, north of Parker Dam, where foramini- lower part of the Bouse Formation, foraminif- foraminiferal species. The benthic foraminif- fers have not been found; (2) in the northern eral diversity patterns and species are more eral assemblages include species of Ammonia, part of the Blythe basin, from Parker Dam to the consistent with marine environments similar Bolivina, Cibicides, Elphidium, Eponidella, Big Maria Mountains, where diversity is fi ve or to estuaries. An estuary is defi ned as a coastal Protoelphidium, Quinqueloculina, and Rosa- fewer species; and (3) the southern part of the body of water with free communication to the lina (Smith, 1969, 1970; Winterer, 1975; Blythe basin, where as many nine species per ocean and within which ocean water is diluted McDougall , 2008a, 2011). Agglutinated species sample are found (Fig. 3). With few exceptions, by freshw ater derived from land (Valle-Levinson, are less common, but include Haplophrag- diversities are limited to one species per sample 2010). Above 110–116 m asl in the Bouse For- moides and Trochammina. A rare occurrence of at any elevation above sea level. Exceptions mation of the Blythe basin, foraminiferal diver- Uvigerina in Mf11676 is also noted. The most to the north-south and elevation patterns are: sity patterns and species are more consistent diverse assemblages are found in the lower part (1) fi ve benthic foraminiferal species noted in with lacustrine environments similar to a saline of the LCRP wells and Hart Mine Wash sec- the northern part of the Blythe basin at 63–65 m lake. A saline lake is defi ned as a large body of tion, whereas assemblages from spot samples asl in Mf11677 and Mf11684, (2) two species water without connection to the sea in geologi- at higher elevations contain a single species, at 110 m asl in the Big Maria Mountains area cally recent time and with high salt concentra- Ammonia beccarii. (Big Maria Quarry and sample Mf11680), and tions (Hammer, 1986).

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TABLE 2. DISTRIBUTION OF MICROFOSSILS IN PREVIOUSLY PUBLISHED BOUSE LOCALITIES IN CALIFORNIA AND ARIZONA FROM SMITH (1970) AND WINTERER (1975)

USGS Micrpaleontology Laboratory numbers Mf11681 Mf11691 Mf11692 Mf11693 Mf11680 Mf11694 Mf11682 Mf11683 Mf11675 Mf11674 Mf11685 Mf11686 Mf11690

Field numbers LCRP 3-187-6 LCRP EU 1-64-21 EU 1-64-22 4-48-9 LCRP 4-48-18 LCRP AMS 4968-2 1-38-1 LCRP 1-38-2 LCRP 2-21-16 HA 2-21-17 HA Col. 1-99-1 Col 1-98-1 J209 J210 J212 J217 LCRP 1-179-1 LCRP

Elevation (m) 170.7 167.6 189.0 231.6 115.8 182.9 121.9 115.8 158.5 158.5 128.0 106.7 121.9 109.7 140.2 88.4 182.9 Ammonia beccarii 1079 16251847 1031 73 AA AA Bolivina subexcavata 130 22 Cibicides lobatulus 3 Eponidella palmerae 4 43 Eponidella sp. R Elphidium cf. E. poeyanum C Lenticulina sp. 1 Neoconorbina terquemi 13 Protoelphidium sp. R† R† 54 Benthic foraminifers Rosalina columbiensis F† 1 202 135 Trochammina sp. R† Globigerina sp. (= juvenile A. beccarii) R* Globorotalia sp. 1 1 Neogloboquadrina sp. 1 1 Streptochilus subglobigerum 2

Planktic Streptochilus subglobigerum-latus 3 foraminifers Streptochilus latus 1 Diatoms A Ostracodes, no identiﬁ cation R A Cyprideis sp. R X Ilocypris sp. or Limnocythere sp. R X R C A Candona sp. X X R

Ostracodes Cytheromorpha sp. X R Mulinia sp. X Halodakra sp. X X X Corbicula sp. X Batillarla sp. X X X X Melania or Goniobasis sp. X Barleeia sp. X X Hydrobidae X Physa X

Mollusks Fontelicella sp. X X R X Ranzia cf. R. lecontei X Tryonia sp. X Macoma sp. X X Diplodonta sp. X X Bittium sp. X X Barnacles (Balanus subaldibus or B. canabus) X X XXX XX Crustaceans X X Chara AA Note: USGS—U.S. Geological Survey. Abundances are given in actual number of specimens counted or R = 1 specimen; F = 2–10 specimens; C = 10–20 specimens; A = >20 specimens; AA = >50 specimens; and X = present. Elevations above sea level are given as positive numbers. *Reported in Winterer (1975) but not seen in slide or in Smith (1970). †Not seen on slide examined in USGS Micropaleontology Collection (Flagstaff, Arizona).

Benthic foraminiferal composition indicates These shallow inner neritic faunas occur in neritic faunas (Bandy, 1961; Walton, 1955). In that deposition initially occurred at shallow the Hart Mine Wash section at elevations of the San Francisco Bay, similar living assem- inner neritic depths (≤50 m), based on the pres- 110–126 m asl. Differential movement between blages are found in the deep western bay estua- ence of Ammonia beccarii, Bolivina subexca- the mountains east of Cibola and the center of rine cluster of McGann (in Chin et al., 2010) at vata, Elphidium poeyanum, Eponidella palm- the Palo Verde Valley (under the city of Blythe) water depths ranging from 14 to 49 m. Arnal erae, Neoconorbina terquemi, Protoelphidium is between 300 and 600 m, thus the Hart Mine et al. (1980) described a fauna including Ammo- sp., Rosalina columbiensis, and various agglu- Wash sediments probably correlate with sedi- nia beccarii, Elphidium, rare Bolivina and tinated forms. This fauna, together with rare ments at a lower elevation and the original Buliminella, in which agglutinated species are planktic foraminifers, occurs at the lowest elevation at the time of deposition is unknown. rare or absent, in a deep channel of the southern elevations of the southern Blythe basin and last The foraminiferal faunas found at the low- San Francisco Bay, where water depths range appears at 123 m asl (Fig. 4). Above 126 m the est elevations and assumed to be the oldest are from 12 to 22 m and ocean water is present year foraminiferal fauna is restricted entirely to a similar to faunas observed in the modern Gulf round. Both areas and assemblages contain rare single species, A. beccarii. of California in the lagoons, beach, and inner planktic foraminifers. In general this group of

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TABLE 3. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN HART MINE WASH, ARIZONA

USGS Micropaleontology Laboratory number Mf12915 Mf12916 Mf12917 Mf12918 Mf12936 Mf12935 Mf12925 Mf12912 Mf12913 Mf12914 Mf12920 Mf12921 Mf12919

Field number 04241307-D 04241307-E 04241307-F 04241307-G1 09201303-B 09201303-A 04241307-I 04241307-A 04241307-B 04241307-C 04241307-H 4241306 04241307-G2

Elevation (m) 115.4 118.2 121.2 123.0 <110 <110 112.4 112.8 114.0 114.0 126.0 >126 123.7 Ammonia beccarii 713 24 44 181 31 5 5 13 4 22 22 12 Bolivina paciﬁ ca 1 1 Bolivina subexcavata 1 Bolivina sp. 1 Cibicides ﬂ etcheri 1 1 1 Cymbaloporetta cf. C. milletti 1 Elphidium cf. E. gunteri 1 Eponidella palmerae 3 1 Haplophragmoides sp. 1 Neoconorbina tequemi 1 Rosalina columbiensis 1 9 62 173 5 Spirilina vivipara 1 1 Streptochilus latus 249 5 10 Streptochilus subglobigerus 3 12 1 Streptochilus sublobigerus-latus 9 54 5 5 Streptochilus sp. 1143 Diatoms (pyrite) R A Chara F Ostracods F C C F F F R R Note: USGS—U.S. Geological Survey. Abundances are given in actual number of specimens counted. R = 1 specimen; F = 2–10 specimens; C = 10–20 specimens; A = >20 specimens.

species is commonly found in shallow (water petitor and thrives best where it lacks compe- abnormalities (~1%), and abnormalities of 5% depth 0–12 m) to intermediate (water depth tition (Arnal, 1961). The presence of juvenile or more are reported from tide pools and coastal 12–30 m) assemblages along the west coast of specimens of A. beccarii throughout the Bouse lagoons with intermittent marine connections North America (Lankford and Phleger, 1973). In Formation indicates that temperature and salin- (Arnal, 1955), whereas under hyposaline or the Puget Sound area, the foraminiferal assem- ity conditions remained within the limits toler- hypersaline conditions abnormalities can affect blage includes more agglutinated species than ated by this species. Laboratory experiments and 50% or more of the population (Stouff et al., currently found in the Bouse Formation (Cush- fi eld observations indicate that normal growth 1999). Increased percentages of abnormal tests man and Todd, 1947; Cockbain, 1963; R.A. and reproduction in A. beccarii occurs between are noted in saline lakes worldwide (e.g., Resig Harman, 2001, personal commun.). temperatures of 17 and 32 °C, and salinities of 1974; Cann and de Deckker, 1981; Almogi- Ammonia beccarii is abundant and dominates 15‰–40‰ (Bradshaw, 1957, 1961; Schnitker, Labin et al., 1992; Le Cadre et al., 2003), and the upper part of the Bouse Formation in the 1974; Walton and Sloan, 1990). the identifi cation of this pattern in the upper Blythe basin (Fig. 5). In samples at elevations In the Blythe basin, some A. beccarii speci- part of the Bouse Formation could suggest the below 100 m asl, A. beccarii rarely exceeds 100 mens were deformed with abnormalities that presence of a similar environmental setting. specimens or few to rare specimens in sam- include double tests, protuberances on the However, additional study is needed before ples where only relative abundance data exist. spiral side, or an unusual chamber arrange- test deformity can be used to determine salinity Samples where relative abundances indicate an ment. The number of deformed A. beccarii changes in the Bouse Formation, because many increase in the number of A. beccarii specimens specimens in the Bouse Formation increases samples are missing. are clustered in two intervals: –129 to –164 m from an average of <1% of the population at Planktic foraminifers in the Bouse Forma- bsl in Mf11678 and at –121 to –152 m bsl in elevations below sea level to 2.9% of the popu- tion are primarily restricted to southern part Mf11676; and at 49 and 64 m asl in Mf11684 lation at elevations between sea level and 100 of the Blythe basin (Tables 2–11; Fig. 3). The and 55–56 to 63 m asl in Mf11677. Maximum m asl, and decreases to 1.72% of the population specimens are usually rare; some are well pre- abundances of 137–179 specimens per sample above 100 m asl (Fig. 6). The higher number served, while others are fragmented but still pre- were found in Mf11678 samples at –143 to of deformities in the interval between sea level serve a distinctive delicate wall texture. Species –146 m bsl. At elevations above 100 m in the and 100 m asl may refl ect the unstable salinities belonging to the genera Globorotalia, Neoglo- Blythe basin (especially in the northern part), in this interval. Test abnormalities in A. bec- boquadrina, Streptochilus, and Tenuitellita are the abundance of A. beccarii ranges from zero carii are common when there are variations in recognized in the foraminiferal assemblages. to much greater than 100 specimens per sample environmental parameters such as temperature Specimens identifi ed as Globigerina sp. in Big (maximum abundance >2000 specimens per or salinity (Arnal, 1955; Resig, 1974; Cann and Maria Quarry, in several of the LCRP wells, and sample). The higher abundances of A. beccarii de Deckker, 1981; Almogi-Labin et al., 1992; in the Bristol basin (Danby and Cadiz wells) by are probably due to environmental changes that Stouff et al., 1999; Debenay et al., 2001; Wenn- Smith (1970) are in fact juvenile A. beccarii. eliminated other benthic foraminiferal species, rich et al., 2007). Under normal marine salinity, Only one planktic foraminifer was identifi ed because A. beccarii is an extremely poor com- A. beccarii populations have a low number of in the northern part of the basin (Mf11677),

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TABLE 4. DISTRIBUTION OF MICROFOSSILS IN NEW LOCALITIES FROM THE BOUSE FORMATION, CALIFORNIA AND ARIZONA

USGS Micropaleontology Laboratory number Mf10506 Mf10507 Mf10508 Mf10514 Mf2755 Mf2756 Mf10501 Mf10502 Mf10503 Mf10504 Mf10505 Mf10509 Mf10510 Mf10513 Mf2752 Mf2754

Field number 00KM13 powder MWC-61-74 00KM14A (top) 00KM14A MWC-62-74 00KM2 marl 00KM3 00KM7 00KM8 00KM9 00KM4 lower marl 00KM5 00KM6 00KM10 00KM11 MWC-58-74 MWC-60-74 Elevation (m) 152.4 152.4 152.4 152.4 121.9 121.9 121.9 121.9 118.9 118.9 118.9 118.9 118.9 118.9 103.6 85.3 Ammonia beccarii 74 32 54 67 229 392 434 156 60 472 857 Diatoms Ostracodes X XXXXXXXXXXXXX X Micromollusks X X XXXX shell fragments X X X X Chara X X X X Fish debris

USGS Micropaleontology Laboratory number Mf10522 Mf10523 Mf12073 Mf12074 Mf12077 Mf10524 Mf12068 Mf12069 Mf 12087 Mf10515 Mf10516 Mf10517 Mf10518 Mf10519 Mf10520 Mf10521

Field number 00KM18B (bag 2) oat material near KM14 ﬂ DM-06-331-17 DM-06-331-18 DM-06-331-21 00KM19 DM-06-331-7 DM-06-331-9 M08AM-166-12 00KM14B (bottom) 00KM15 00KM15A 00KM16 00KM17 00KM18A (top) 00KM18A 00KM18B (bag 1) Elevation (m) 85.3 115.8 115.8 121.9 85.3 85.3 85.3 85.3 85.3 140.2 137.2 115.8 112.8 109.7 85.3 Ammonia beccarii 18 106 91 20 161 8 50 524 712 Diatoms X Ostracodes X XXXXXXX XXXXX X Micromollusks XX X shell fragments X X X Chara X X X X Fish debris X X X

USGS Micropaleontology Laboratory number Mf 12092 Mf 12093 Mf 12098 Mf12857 Mf 12088 Mf 12089 Mf 12090 Mf 12091 Mf 12094 Mf 12095 Mf 12096 Mf 12097 Mf12858 Mf12859 Mf12860 Mf12862

Field number M08AM-166-110 M08AM-166-125 M08AM-166-245 2012-KM-1 M08AM-166-45 M08AM-166-65 M08AM-166-80 M08AM-166-95 M08AM-166-135 M08AM-166-150 M08AM-166-180 M08AM-166-215 Bouse 12-12 Beard #1 Beard #2 2012-KM-3 Elevation (m) 85.3 85.3 85.3 85.3 85.3 85.3 85.3 85.3 85.3 85.3 85.3 109.7 121.9 121.9 121.9 121.9 Ammonia beccarii 321 310 370 386 422 Diatoms X XXXXXXXXXX Ostracodes X XXXXXXXXXXXX X Micromollusks X XXXXXXXXXX shell fragments XXX Chara Fish debris

USGS Micropaleontology Laboratory number Mf12889 Mf12890 Mf12891 Mf12892 Mf12899 Mf12901 Mf12902 Mf12896 Mf12897 Mf12898 Mf12903 Mf12906 Mf12863 Mf12864

Field number 4041303-2 4031303-3 4061311 4061312-B kh-10301208a 4061312-C 4081303 kh-10311219 kh-11021205 2071304-05 2071310 4071310 2012-KM-4 2012-KM-5 Elevation (m) 121.9 179.8 304.8 304.8 304.8 195.7 243.8 304. 8 292.6 292.6 152.4 146.3 152.4 280.2 Ammonia beccarii 239 35 346 309 368 287 Diatoms Ostracodes X XXXXXXXXXXXXX Micromollusks XXXXX shell fragments X Chara X Fish debris Note: USGS—U.S. Geological Survey. Abundances are given in actual number of specimens counted or by an X = present. Elevations above sea level are given as positive numbers.

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TABLE 5. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN BIG MARIA QUARRY, CALIFORNIA

USGS Micropaleontology Laboratory number Mf444 Mf443 Mf442 Mf456 Mf455 Mf454 Mf453 Mf452A Mf452 Mf451 Mf447 Mf446 Mf445 Mf441 Mf420 Mf449 Mf448A Mf448 Mf450

Field number BMG-4 BMG-3 BMG-2 BMG-16 BMG-15 BMG-14 BMG-13 BMG-12A BMG-12 BMG-11 BMG-7 BMG-6 BMG-5 BMG-1 A-1 BMG-9 BMG-8A BMG-8 BMG-10 Ammonia beccarii 26 126 666 292 279 2136 74 A 145 1136 1855 156 444 35 71 F 34 328 992 Rosalina columbiensis F Ostracodes F A C C F F F C AAAACAAFFFF Mollusk fragments F Chara C F A Ooliths F Note: USGS—U.S. Geological Survey. Elevation of the quarry is 109.7 m above sea level. Abundances are given in actual number of specimens counted, or F = 2–10 specimens; C = 10–20 specimens; A = >20 specimens.

but the isolated occurrence and poor preser- bigerinids are present in the Straits of Juan de Streptochilus can live deeper in the upper water vation makes this identifi cation questionable Fuca, near the U.S.-Canadian border along the column in temperate to tropical, highly produc- (Plate 1). Scanning electron microscope photo- Pacifi c coast, but are rare in the Rosario Straits tive waters or in shallow surface waters close to graphs revealed that some of the specimens fi rst and are not present in the Straits of Georgia or upwelling zones in coastal regions (Resig and identifi ed as the benthic foraminifer Bolivina in the southern part of Puget Sound (Cushman Kroopnick, 1983; Hemleben et al., 1989; Smart subexca vata by Smith (1970) are the planktic and Todd, 1947; Cockbain, 1963; R.A. Harman, and Thomas, 2006). foraminifer Streptochilus, based on the aperture 2001, personal commun.). In San Francisco The change to monospecifi c foraminiferal and wall texture (Plate 1). Bay, northern California, Globigerina bulloides assemblages (~110 m asl), increased abun- Streptochilus has been ignored in plank- occurs rarely in the entrance to the bay and in dance of Ammonia beccarii (~110 m asl), and tic assemblages and biostratigraphic analysis the central bay, just west of the Golden Gate absence of planktic foraminifers above 123 m because of its misidentifi cation as a benthic Bridge (Arnal et al., 1980; Chin et al., 2010). asl in the Bouse Formation coincide with the foraminifer, its small size (63–125 µm), and pre- In the Gulf of California, planktic species are lowest occurrences of Chara, a green algae. viously unproven stratigraphic value (Kennett common in outer shelf water depths and deeper, Chara were observed in foraminiferal resi- and Srinivasan, 1983; Resig, 1989). A complete but are missing from large areas of the Gulf of dues in a sample at the top of the Hart Mine and well-preserved fossil record in the western California, including the Colorado River delta, Wash section (~126 m asl), Milpitas Wash Pacifi c and Indian Ocean has allowed recogni- due to rainfall and run off, which cause salin- (85 m asl), Big Maria Quarry, (110 m asl), tion of the biostratigraphic relevance of this ity variations (Walton, 1955; Bandy, 1961). and Bouse Wash (116–152 m asl) (Fig. 7). genus (Resig, 1989, 1993). Planktic species most tolerant of hyposaline This algae is common in shallow freshwater, In the Blythe basin, Streptochilus cf. S. sub- conditions (salinities range of 30.5‰–31‰) and some species can tolerate brackish-water globigerum specimens have a broken last cham- are Globigerina bulloides, G. quinqueloba, conditions with salinities approaching 20‰ ber. Although wall texture in the fi nal chamber Globigerinita uvula, Globigerinoides ruber, (Olsen, 1944; Wood, 1952; Proctor, 1961; is an important characteristic with which to dis- Neogloboquadrina pachyderma (f. superfi cia- Burne et al., 1980). Its presence supports a tinguish this species from the younger species ria), and Orbulina universa (Be and Tolderlund, saline lake interpretation for the upper part of S. globigerus, other characteristics that allow the 1971). These hyposaline tolerant species are the Bouse Formation. taxonomic identifi cation are the good preserva- absent in the Bouse Formation in the Blythe The presence of reworked Cretaceous micro- tion of fi nely cancellate wall texture (images 24 basin, whereas species common in normal fossils derived from the Mancos Shale in the and 25 in Plate 1), straighter sutures, and less marine salinities like Streptochilus are present Bouse Formation indicates the presence of globular chambers than S. globigerus specimens (Darling et al., 2009; De Klasz et al., 1989). Colorado River water. According to Winterer (Plate 1). These characters were described by Living Streptochilus are present principally in (1975), D.G. Metzger (1975, personal com- Resig (1989) for juvenile stages of S. subglobig- surface marine waters (Darling et al., 2009; De mun. in Winterer, 1975) reported Cretaceous erum and later forms transitional to S. latus spe- Klasz et al., 1989; Smart and Thomas, 2006), coccoliths in Bouse Formation outcrops from cies are also present in the Blythe basin. although oxygen isotope values suggest that Needles to Chemehuevi Valley. Paul Fritts Laboratory experiments indicate that some species of planktic foraminifers can toler- TABLE 6. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN Mf11679 ate greater variations in salinity than occurs in modern oceans (Hemleben et al., 1989; Bijma

et al., 1990; Lee et al., 2010); e.g., Neoglobo- Elevation Well Depth Well depth beccarii quadrina dutertrei can tolerate salinities rang- (m) (feet) (m) ing from 24‰ to 46‰ in the laboratory (Bijma Ammonia Ostracodes et al., 1990). Regardless of this broader toler- Mollusks ance range, planktic foraminifers are absent 93.57 208–212 63.40–64.62 X 82.90 243–258 74.07–78.64 X from saline lakes that have no connection with 75.59 267–271 81.38–82.60 7 X X marine waters, are extremely rare in saline lakes Note: U.S. Geological Survey Micropaleontology Laboratory number Mf11679.The well head with marine connections, and are rare in estua- is at an elevation of 157 m and total depth drilled was 158.5 m. Abundance is actual number of rine environments. For example, living glo- specimens counted , or X = present. Elevations are above sea level.

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TABLE 7. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN Mf11678 sp. Elevation Well depth Well depth ? sp. E. gunteri sp. B. subexcavata

(m) (feet) (m) palmerae sp. cf. cf. Globigerina Ostracodes Mollusks Buliminella Cribroelphidium Eponidella Elphidium Quinqueloculina Ammonia beccarii Bolivina Rosalina columbiensis –89.92 535–545 163.07–166.12 R –94.49 550–552 167.64–168.25 R –95.10 552–560 168.25–170.69 R R –97.53 560–565 170.69–172.21 R –99.06 565–570 172.21–173.74 R –100.59 570–575 173.74–175.26 F R R –102.11 575–580 175.26–176.78 F R –103.63 580–585 176.78–178.31 R R R R –105.16 585–590 178.31–179.83 F R R –106.68 590–595 179.83–181.36 R R –108.21 595–600 181.36–182.88 R R R –109.73 600–605 182.88–184.40 R R R –112.78 610–615 185.93–187.45 R –114.30 615–620 187.45–188.98 R –115.83 620–625 188.98–190.5 F R R R –117.35 625–630 190.5–192.02 R R –118.87 63–635 192.02–193.55 F F R –120.40 635–640 193.55–195.07 R R –121.92 640–645 195.07–196.60 R R R –123.45 645–650 196.6–198.12 F R R –124.97 650–655 198.12–199.64 R R R –126.49 655–660 199.64–201.17 R R –128.02 660–665 201.17–202.69 F F R –129.54 665–670 202.69–204.22 C R F R R R R –131.07 675–680 204.22–207.26 C F F R R –134.11 680–685 207.26–208.79 C F R R R R –135.64 685–690 208.79–210.31 F R R R R R –137.16 690–700 210.31–213.36 F R R F –140.21 700–705 213.36–214.88 F R R R –141.73 705–710 214.88–216.41 31 1 5 6 –143.26 710–715 216.41–217.93 137 1 2 46 18 2 R F –144.78 715–720 217.93–219.46 186 2 14 4 F F –146.31 720–725 219.46–220.98 185 1 72 26 2 2 F R –147.83 725–730 220.98–222.50 C F F F R –149.35 730–735 222.50–224.03 A R C F F F R F –150.88 735–740 224.03–225.55 A R C F R C F –152.40 740–745 225.55–227.08 A C F R R C R –153.93 745–750 227.08–228.6 A C R R R C R –155.45 750–755 228.6–230.12 R R –156.97 755–760 230.12–231.65 F F C –158.50 760–765 231.65–233.17 A A F R –160.02 765–770 233.17–234.70 R F R R R –161.55 770–775 234.70–236.22 C F F F F R F R –163.07 775–780 236.22–237.74 A F C C F R R –164.59 780–785 237.74–239.27 A A C F C A F –166.12 785–790 239.27–240.79 F A R R R –167.64 790–795 240.79–242.32 F R F R C F –169.17 795–800 242.32–243.84 R R F F R Note: Sample Mf11678. The well had is at an elevation of 73.2 m and a total depth of 243.8 m was drilled. Abundances are given in actual number of specimens counted, or R = 1 specimen; F = 2–10 specimens; C = 10–20 specimens; A = >20 specimens. Elevations of samples below sea level are given as negative numbers.

(1975, personal commun., in Winterer, 1975; from the Vidal wells (B-30, J40 and B-30, J64) staff, Arizona), Smith indicated that Cretaceous and Fritz, 1975, unpublished report provided by correspond to elevations of 188 and 157 m coccoliths were found in the Big Maria Quarry K. Howard, 2012, personal commun.) reported asl. Winterer (1975) reported that there are no samples (Mf441 to Mf456) at an elevation of reworked Cretaceous coccoliths in the Bouse cocco liths in the basal marl of the Bouse Forma- 110 m asl. Formation from the subsurface near Blythe, Ari- tion near Cibola (locality J217, samples C2–12, The presence of reworked Cretaceous cocco- zona. No depths or locations were given. Smith elevation 140.2 m asl). Lucchitta (1972) implied liths at elevations of 110 m asl and higher, and (1970; and in Lucchitta, 1972) reported that that although no Mancos-type foraminifers have primarily in the northern part of the Blythe there are no reworked microfossils in the sub- been found in the Bouse Formation, coccoliths basin, indicates the presence of sediment surface samples she examined of the Bouse For- were found in surface exposures of the unit; derived from the Mancos Shale, most likely by mation. Winterer (1975) also reported cocco- however, no locations were given. In a memo the Colorado River. This distribution resem- liths from three samples: one surface sample in from P. Smith to D. Bukry dated 20 May 1968 bles the distribution of Chara (Fig. 7), and the the Needles area, and two subsurface samples (USGS Micropaleontology collection, Flag- occurrences are in the interval interpreted to be

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TABLE 8. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN Mf11677 spp. sp. sp. Elevation Well depth Well depth E. gunteri B. subexcavata (m) (feet) (m) sp. beccarii cf. subexcavata cf. Haplophragmoides Quinqueloculina Rosalina columbiensis Globigerina Neogloboquadrina Ostracodes Mollusks Bolivina Eponidella palmerae Elphidium Ammonia Bolivina 63.09 125–150 38.1–45.72 A F C C F C R 56.38 147–148 44.81–45.11 C R X X 55.47 150–175 45.72–53.34 F R 47.85 175–200 53.34–60.96 R 40.23 200–225 60.96–68.58 R –28.35 ~425 ~129.54 F –79.56 593–594 180.75–181.05 1 1 1 1 –81.69 ~600 ~182.88 F R Note: Sample Mf11677. The well head is at an elevation of 101.2 m and a total depth of 232.6 m was drilled. Abundances are given in actual number of specimens counted, or R = 1 specimen; F = 2–10 specimens; C =10–20 specimens; A = >20 specimens; X = present. Elevations of samples above sea level are given as positive numbers; elevations of samples below sea level are given as negative numbers.

TABLE 9. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN Mf11689

Elevation Well depth Well depth

(m) (feet) (m) sp. Ammonia beccarii Bolivina subexcavata Cibicides –28.96 ~625 ~190.5 F C R Note: The well head is at an elevation of 161.5 m and a total depth of 304.8 m was drilled. Abundances: R = 1 specimen; F = 2–10 specimens; C =10–20 specimens. Elevations of samples below sea level are given as negative numbers.

TABLE 10. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN Mf11676 vars.

Elevation Well depth Well depth sp. (m) (feet) (m) S. subglobigerum T. iota T. cf. sp. sp. cf. palmerae columbiensis sp. subexcavata Mollusks Ooliths Fish teeth Ammonia beccarii Bolivina Cibicides Uvigerina peregrina Globigerina Globorotalia Neogloboquadrina Streptochilus Eponidella Rosalina Tenuitellita Tenuitellita 15.24 250–300 76.2–91.44 R R R 0.00 300–350 91.44–106.68 R R –15.24 350–400 106.68–121.92 R –30.48 400–450 121.92–137.16 R R –45.72 450–500 137.16–152.4 R –48.46 459–499 139.90–152.10 11 1 –60.96 500–550 152.4–167.64 R R –76.20 550–600 167.64–182.88 R R R –91.44 600–650 182.88–198.12 R –106.68 683–689 208.18–210.01 2 1 14 26 1 2 2 1 1 X X X –116.74 650–700 198.12–213.36 R R R –121.92 700–750 213.36–228.6 C F R R –137.16 750–800 228.6–243.84 C R R R R –152.40 >800 >243.84 C R R Note: The well head is at an elevation of 91.4 m and a total depth of 304.2 m was drilled. Abundances are given in actual number of specimens counted, or R = 1 specimen; F = 2–10 specimens; C =10–20 specimens; X = present. Elevations of samples above sea level are given as positive numbers; elevations of samples below sea level are given as negative numbers.

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TABLE 11. DISTRIBUTION OF MICROFOSSILS FROM THE BOUSE FORMATION IN Mf11684 and Puget Sound have much higher diversities and diversity increases with depth. Diversities of 20 or more species occur in the central Gulf of California (Bandy, 1961). In San Francisco Elevation Well depth Well depth sp. Bay, diversities increase from ~9 species/sample E. gunteri (m) (feet) (m) R. columbiensis B. subexcavata in the nearshore areas to 14 or more species/ cf. cf.

cf. sample in the deeper central areas (Arnal et al., 1980; Chin et al., 2010). A similar pattern occurs in Puget Sound, where the highest diversities are Ostracodes Mollusks Rosalina Elphidium Quinqueloculina Ammonia beccarii Bolivina subexcavata Bolivina 64.62 100–150 30.485.72 A R C R C found in the central area of the straits and away 49.38 150–200 45.72–60.96 C from the shoreline (Cockbain, 1963). 34.14 200–250 60.96–76.2 R 18.90 250–300 76.2–91.44 Distribution and composition patterns of 3.66 300–350 91.44–106.68 foraminifers from estuaries exhibit biofacies –11.58 350–400 106.68–121.92 patterns that parallel the shoreline and change –26.82 400–450 121.92–137.16 R –42.06 450–500 137.16–152.4 R with depth or distance from the shoreline. In –57.30 500–550 152.4–167.64 contrast, patterns in saline lakes tend to be more –72.54 550–600 167.64–182.88 –85.65 593–594 180.75–181.05 X X uniform, do not change with depth or distance –85.95 595–604 181.05–184.10 X X from the shoreline, and are affected primarily –87.78 600–650 182.88–198.12 F R by the infl ux of river water (Arnal, 1961; Chin –104.24 654–657 199.34–200.25 X X –116.13 693–702 211.23–213.97 X X et al., 2010). Agglutinated faunas are common Note: The well head is at an elevation of 95.1 m and a total depth of 292.1 m was drilled. Abundances are given in marine estuaries and embayments (Bandy, in actual number of specimens counted, or R = 1 specimen; F = 2–10 specimens; C = 10–20 specimens; A = >20 1961; Cockbain, 1963; Ellison and Nichols, specimens; X = present. Elevations of samples above sea level are given as positive numbers; elevations of samples below sea level are given as negative numbers. 1970; Arnal et al., 1980; R.A. Harman, 2001, personal commun.). The presence of planktic foraminiferal species in the foraminiferal fauna is a good indica- deposited in a saline lake by the foraminiferal a marine environment include diversity patterns, tor for discriminating marine shelf, estuarine, assemblages. The absence of reworked microfaunal composition and distribution patterns of and saline lake deposits. Planktics are absent in fossils at lower elevations suggests that the benthic foraminifers, abnormal tests, endemism , saline lakes, rare in estuarine environments, and Colorado River was not eroding the Mancos and the presence or absence of planktic fora- common in the outer shelf biofacies of marine Shale or it was not a major source of sediment minifers. These criteria are based on compari- environments. They are sensitive to salinity in the Blythe basin. sons of saline lakes and several marine estuar- changes and are therefore missing from large ies (Straits of Juan de Fuca, Straits of Georgia, areas of the Gulf of California because of river SALINE LAKE VERSUS MARINE Puget Sound, San Francisco Bay, and the Gulf input and runoff. A similar situation occurs in ORIGIN OF THE BOUSE FORMATION of California) as listed in Table 12. the Straits of Georgia, British Columbia, Can- Foraminiferal faunal diversities in saline ada, where planktics and many benthic species Although the Bouse Formation foraminiferal lakes are generally low and contain many of the are not present in the marine assemblages north associations suggest an initial marine environ- same species as the local marine environment, of the Fraser River delta. In the San Francisco ment, it has been argued that the foraminifers whereas estuaries have higher diversities that Bay, planktic foraminifers occur only rarely were introduced by avian transport to a saline increase away from the shoreline. The number east of the Golden Gate Bridge. In both cases lake (Spencer and Patchett, 1997; Spencer of foraminiferal species in shallow saline lakes the absence is due to the infl ux of freshwater. et al., 2005, 2008, 2013). Saline lakes occur is consistent across the lake, whereas in larger Abnormal, deformed, or dwarfed tests can in a wide variety of settings and many con- lakes with greater depths, diversity decreases also be used to differentiate saline lakes from tain foraminiferal faunas (Fig. 8). A survey of toward the center due to the increase in organic marine estuaries. Abnormal or deformed Ammo- saline lakes worldwide shows that if foramini- carbon content and the decrease in pH of the sed- nia tests occur ~1% of the time in normal saline fers are present, they were introduced either as iment (Arnal, 1961; Chin et al., 2010). With few conditions but there is a high rate of abnormali- an in situ component (i.e., the lake was origi- exceptions the foraminiferal fauna in saline lakes ties under both hypersaline and hyposaline con- nally part of the sea or is periodically fl ooded that have had no connection with marine waters ditions (Stouff et al., 1999; Debenay et al., 2001; by the sea) or through avian transport. Avian usually contain fi ve or fewer species (Bach huber Wennrich et al., 2007). Dwarfi sm, which is pres- transport of foraminifers can be a successful and McClellan, 1977; Cann and de Deckker, ent in marine environments, is usually the result dispersal mechanism to colonize new habitats 1981; Anadon, 1989; Kázmér, 1990; Patterson of low oxygen conditions and is frequently (Patterson et al., 1997); a small population of et al., 1997; Giralt et al., 1999; Boudreau et al., accompanied by other indicators of low oxygen foraminifers is transported by birds and even a 2001; Wennrich et al., 2007). Exceptions include such as low oxygen species and enlarged pores smaller number survive the new environmental the Salton Sea with 21 species (Arnal, 1954, on the tests (Douglas, 1979). Dwarfed benthic conditions to colonize the new habitat. Although 1958, 1961) and the Salt Lake in Hawaii with 41 foraminiferal faunas can be found living below this small population may give way to a much species (Resig, 1974). Lakes that have a marine sill depth in marine basins in the Gulf of Califor- larger population, the probability is low that connection at some point in their existence have nia (Bandy, 1961). the initial foraminifers will survive and become higher diversities, including some species not Endemism and isolated occurrences can be a part of the fossil record. Criteria to differentiate found in the isolated saline lakes. Estuaries such diagnostic criterion of a saline lake. If the benthic saline lakes with transported foraminifers from as the Gulf of California, San Francisco Bay, foraminiferal species adapt to the environmental

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S. Blythe Basin N. Blythe Basin Chemehuevi and Mohave-Cottonwood Basins 600 560 m = highest Bouse Fm.

500

400

330 m = highest Bouse Fm. 350 m = highest Lawlor Tuff 300 Bouse Fm. Hart Mine Wash Osborne Davis Milpitas Bouse Wash 200 Dam Wash Wash Big Maria Topock Quarry Elevation (m) Parker Gorge Mf11682 Mf11680 Dam 100 Mf11683 Diversity

Sea Level 6 0 5 4 Mf11679 –100 3 2 –173 m = 1 deepest Bouse Fm. –200 Mf11677

Mf11689 0 Planktic Mf11678

Mf11684 foraminifers –300 Mf11676 33.00 33.50 34.00 34.50 35.00 35.50 South North

Latitude

Figure 3. Diversity (species/sample) of benthic foraminiferal assemblages and the presence of planktic foraminifers plotted with respect to elevation and latitude. Diversity distribution suggests three geographic groupings: north of Parker Dam (Chemehuevi, Mohave, and Cottonwood basins), northern Blythe basin from Parker Dam to the Big Maria Mountains, and southern Blythe basin from the Big Maria Mountains to the Chocolate Mountains. Benthic foraminiferal diversity generally decreases with elevation. Exceptions are assemblages found at elevations of 115–123 m in the Hart Mine Wash. Benthic foraminiferal assemblages in this interval reach a maximum diversity of nine species per sample and planktic foraminifers are present in four samples. The basin contour is modiﬁ ed from Turak (2000), Spencer et al. (2008), and Pearthree and House (2014). Lithostratigraphic units in the wells are indicated by color: yellow—Bouse Formation; green—limestone, tufa, and marl beds in the Bouse Formation; gray—pre– and post–Bouse Formation units.

conditions of the saline lake after introduction Benthic foraminiferal diversity in the Bouse from the edges and away from the infl ux of river and if the populations evolve isolated, with time Formation samples is low. The highest diversi- water. The diversity decline with elevation indian endemic fauna could develop. However, if ties are common in the center of the southern cates that the topographically higher (and prob- environmental conditions do not promote sur- Blythe basin (Mf1168 and Mf11676) and in ably younger) part of the Bouse Formation was vival after introduction, the species will be rep- Hart Mine Wash, whereas the lowest diversities deposited in a different sedimentary environ- resented by a single or isolated occurrence. are to the north and along the sides of the basin ment, possibly a saline lake. Applying the criteria to differentiate marine near Parker and in the Bristol basin. The high- Microfossil sampling of the Bouse Formation from saline lake environments to the Bouse For- est diversities are found in the oldest sediments has been random, so there are insuffi cient sam- mation suggests that in Blythe basin both envi- and diversities decrease toward the top of the ples to determine detailed distribution patterns ronments were present. Fossil diversity, compo- outcrop sections and wells (Figs. 3 and 4). This of benthic foraminifers. Nevertheless, faunas in sition, abundances, and deformities indicate that confi guration suggests that initially the Bouse the lower elevations (and probably older) part of the Bouse Formation was initially deposited in a Formation was deposited in a marine estuary the Bouse Formation (Fig. 4) are most similar to marine environment that changed to saline lake rather than a saline lake, because the diversities the inner shelf biofacies of the Gulf of Califor- environment before deposition ended. increase toward the center of the basin, away nia. In contrast, exposures at higher elevations

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spp cf. sp. sp.

E. poeyanum E. gunteri

sp. sp. sp. cf. cf. sp. sp. Diversity

0 2 4 6 8 Spirilina vivipara Ammonia beccarii Bolivina Bolivina subexcavata Buliminella Cibicides lobatulus Cibicides Cribroelphidium? sp. Elphidium Elphidium Eponidella palmerae Eponidella Haplophragmoides Lenticulina Neoconorbina terquemi Protoelphidium Quinqueloculina Rosalina columbiensis Uvigerina peregrina 400 Bolivina pacifica fletcheri Cibicides Cymbaloporetta

300

200 Saline Lake

100 Elevation (m)

Sea level 0 Marine

–100 inner neritic (< 50 m)

–200

planktic foraminifers

Figure 4. Diversity (species/sample) and distribution of benthic foraminiferal assemblages. The diversity and distribution of the benthic foraminifers is plotted with respect to elevation; the last diverse occurrence of benthic foraminifers is between 115 and 123 m above sea level. Above this elevation foraminiferal assemblages are composed of a single species, Ammonia beccarii. The distribution of planktic foraminifers with respect to elevation is also shown.

are dominated by Ammonia beccarii (Fig. 4), lake level reached an elevation of –125 m bsl, ISOTOPES AND MARINE OR and are most similar to the lagoonal biofacies salinity would range from 0‰ to 100‰ and LACUSTRINE DEPOSITION of the Gulf of California (Bandy, 1961) or the while fi lling from an elevation of –125 bsl to saline lake biofacies described from the Salton 64 m asl, salinity would be at 27.6‰. Seawater An additional argument used to support the Sea (Arnal, 1961). The distribution of planktic salinities (35.0‰) would not be achieved until lacustrine origin of the Bouse Formation is foraminiferal species is restricted to the lower shortly before lake level reached 329 m asl. A based on strontium, carbon, and oxygen isotopic part of the formation in the southern Blythe basin fi nal salinity of 35.4‰ just before spillover was ratios. Isotope studies (Spencer and Patchett, (Fig. 3). The highest occurrence of planktic fora- suggested by Spencer et al. (2008). Based on 1997; Spencer and Pearthree, 2001; Poulson minifers, at 123 m asl, approximates the highest this modeling, marine conditions would not be and John, 2003; Roskowski et al., 2010; Spencer occurrence of benthic foraminiferal diversities achieved until the lake was nearly fi lled, whereas et al., 2013) concluded that the Bouse Formation of 2 or more species (116 and 110 m asl) and patterns observed in the benthic foraminifers was deposited in a lake composed of Colorado changes in the abundance and percent deformed indicate that marine salinities were present dur- River water. However, because of the sampling A. beccarii as well as the lowest occurrences of ing the initial deposition of the Bouse Forma- distribution, the isotope data do not contradict a Chara (Fig. 7). These changes suggest a conver- tion in the Blythe basin. Saline lake conditions marine origin for at least part of the Bouse For- sion from marine to saline lake conditions. with salinities lower than normal seawater are mation. Foraminiferal data suggest that marine The predicted salinity model for Lake Blythe evident only in the faunal assemblages found at conditions persisted to an elevation of 123 m asl. (Spencer et al., 2008, 2013) indicates that as the the higher elevations of Bouse Formation. Therefore, the overlap of the marine and fresh-

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A 300

200

100

Sea Level 0

Figure 5. (A) Abundance and distribu- Elevation (m) tion of Ammonia beccarii with respect to elevation in the Blythe basin. –100 Assemblages with only relative abundances were assigned values as fol- lows: R (rare) = 1 specimen, F (few) = 10 specimens, C (common) = 50 speci- –200 mens, and A (abundant) = 100 speci- 0 500 1000 1500 2000 2500 mens. Assemblages with no A. beccarii identiﬁ ed were assigned a value of Ammonia beccarii abundance (number of specimens/sample) zero. Relative abundances indicating an increase in the number of A. beccarii specimens occurs at –129 to –134 m below sea level (bsl), –147 to –153 m bsl and –161 to –164 m bsl in LCRP B Lawlor Tuff 330 m = highest Bouse Fm 16 and at –121 bsl, –137 bsl, and 300 –152 m bsl in LCRP 22 and at 49 and 64 m above sea level (asl), in LCRP 27 Hart Mine and 55–56 and 63 m asl in LCRP 20. Wash Osborne Bouse (B) Cross section of the Blythe basin 200 Milpitas Wash Wash showing the locations of assemblages Wash Big Maria containing 100 or more specimens Quarry of A. beccarii. The basin contour is Mf11682 modiﬁ ed from Turak (2000), Spencer 100 Mf11683 Mf11680 et al. (2008), and Pearthree and House (2014). Lithostratigraphic units in the wells are indicated by color: yellow— Bouse Formation; green—limestone, 0 Sea Level tufa, and marl beds in the Bouse For- mation; gray—pre– and post–Bouse Elevation (m)

Formation units. Mf11679 –100

–173 m = deepest Bouse Fm. –200 Mf11677 Mf11689 Mf11678 Mf11684 Mf11676 –300 33.00 33.50 34.00 Latitude

>100 specimens/sample of Ammonia beccarii

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A 300

250

200

150

100

Elevation (m) 50 Sea Level 0

–50

–100

–150

–200 0.00 1.00 2.00 3.00 4.00 5.00 6.00 7.00 Percentage of deformed A. beccarii specimens Figure 6. (A) Percentage of deformed specimens of Ammonia beccarii plotted with respect to elevation in the Blythe basin. (B) Cross section of the Blythe basin showing the location of assemblages with deformed A. beccarii specimens constitute B Lawlor Tuff 330 m = highest Bouse Fm 300 >1% of the assemblage. The basin contour is modiﬁ ed from Turak (2000), Spencer et al. (2008), and Pearthree and House Hart Mine (2014). Lithostratigraphic units in the wells Wash Osborne Bouse are indicated by color: yellow—Bouse For- 200 Milpitas Wash Wash Wash mation; green—limestone, tufa, and marl Big Maria beds in the Bouse Formation; gray—pre– Quarry and post–Bouse Formation units. Mf11682 Mf11680 100 Mf11683

Sea Level 0 Elevation (m) Mf11679 –100

–173 m = deepest Bouse Fm.

–200 Mf11677 Mf11689 Mf11678 Mf11684 –300 Mf11676 33.00 33.50 34.00 Latitude

Percentage of deformed specimens = >1%

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water conditions suggested by the strontium system and the fact that the lake was only 25% elevations of 100 m or lower contain negative isotopes is limited to an interval between 70 and of capacity so these changes would be clear. δ18O (–2.76‰ to –0.22‰) and δ13C (–0.84‰ 123 m asl. Although isotope samples were taken Because diverse marine benthic and planktic to –0.71‰) values approaching zero. Although from the same sections, they are not the same foraminiferal assemblages occur in the southern interpreted as representing an interval of high samples, and there has not been any coordina- Blythe basin at elevations between 110 and 123 evaporation of freshwater by Roskowski et al. tion between the studies. m asl, the decrease in the strontium values may (2010), these values and a trend toward zero Strontium values from the Bouse Forma- alternatively record a mixing of seawater and (seawater) value could also be interpreted as tion range from 0.7105 to 0.7112 (Buising, river water. The faunal changes above this eleva- including a seawater component. 1990; Spencer and Patchett, 1997; Spencer and tion suggest a saline lake, as do the strontium Other isotope samples from elevations lower Pearthree, 2001; Roskowski et al., 2010; Spen- values. Overall strontium isotopic values in the than 100 m include a sample from Milpitas Wash cer et al., 2013) and are located at elevations ≥70 Bouse Formation are higher than modern river (95 m) and one from the Palo Verde Hills (87 m), m asl with one exception (Fig. 9); Spencer and values but lower than Hualapai Limestone Mem- from which oxygen and carbon isotopes are Patchett (1997) quoted a value of 0.71075 for the ber values (0.713654–0.719536), and suggest strongly negative and approach Colorado River Colorado River based on an analysis by Gold- that there may be additional sources of strontium values. Additional isotopes analysis from Mil- stein and Jacobsen (1988). This value was modi- that were not considered (Crossey et al., 2013). pitas Wash, Palo Verde Hills, and Parker are at fi ed by the analysis of Gross et al. (2001) that Like strontium, the oxygen and carbon iso- elevations higher than 100 m and have negative showed that the modern Colorado River value at topic analyses are primarily from the upper part δ18O values and low δ13C values. These values Lake Mead (Hemenway Harbor, Nevada) was of the Bouse Formation (Fig. 8). Samples ana- may indicate a lacustrine environment. Isotopic 0.710437 and 0.710274 at the Cibola Wildlife lyzed for δ18O and δ13C from the Cibola area and analyses from the bedding plane associated with Refuge, Arizona. Compared to these modern elevations ranging from 70 to 100 m asl plot near the fi sh Colpichthys regis have high negative strontium isotopic values for the Colorado River, seawater, whereas samples from Parker, Milpitas values for δ18O and low δ13C values (Roskowski the late Miocene to Pliocene values are much Wash, Palo Verde Hills, and Limekiln Wash are et al., 2010). Although these samples have eleva- higher and a better understanding of the source from elevations higher than 100 m and are fur- tions (89–99 m asl) similar to the other Cibola and concentration of strontium is needed. ther removed from the seawater values (Poulson area isotope samples, they are northwest of the A single Sr sample analyzed by Spencer and John, 2003; Roskowski et al., 2010) (Fig. other Cibola samples, and the isotope values et al. (2013) from a snail in Mf11684 is from 11). Although Poulson and John (2003) found seem to refl ect evaporation and/or a continental an elevation of –62 m bsl. This specimen and anomalies in their data that indicated an estua- signal, as suggested by Roskowski et al. (2010). others found at –87 m bsl may be Pyrgulopsis rine origin, they concluded that overall the data avernalis (see Spencer and Patchett, 1997), were more consistent with a lacustrine origin. UPLIFT, FLOOD DEPOSITS, AND which is known to inhabit freshwater springs Roskowski et al. (2010) argued that the high COLORADO RIVER SANDS (Hershler, 1994). Its presence in Mf11684 sug- negative δ18O values indicate a continental ori- gests a freshwater spring or transport to this gin for the waters and evaporation of lake waters. Other arguments in favor of a lacustrine ori- location. In addition, the presence of several The values that plot between –5‰ and 0‰ are gin for the Bouse Formation include the pres- freshwater snails (Hydrobiidae?, Fontelicella, believed to represent an interval when lake evap- ence of fl ood deposits attributed to lake overfl ow Physa, and Pyrgulopsis; Smith, 1970; Winterer, oration was high. Samples in the Cibola area at or breakout and the lack of evidence for uplift. 1975; Spencer and Patchett, 1997; Turak, 2000; Spencer et al., 2008, 2013) was noted near the base of the Bouse Formation in Mf11684 (–64, –88, –105, and –119 m bsl) and Mf11677 (–80 Plate 1 (on following page). Scale bars = 50 μm in images 1–23. 1—Juvenile benthic speci- and –83 m bsl) at the northern end of the Blythe men of Ammonia beccarii. Big Maria Quarry, sample Mf452A. 2—Juvenile benthic speci- basin. These freshwater snails occur below the men of Ammonia beccarii. Big Maria Quarry, sample Mf452A. 3—Juvenile benthic speci- fi rst occurrence of foraminifers, suggesting that men of Ammonia beccarii. Big Maria gravel quarry, sample Mf452A. 4—Neogloboquadrina initial deposition in this part of the basin may sp., ventral view, sample Mf11676. 5—Tenuitellita cf. T. iota, lateral view, sample Mf11676. have occurred in a spring or lake prior to the 6—Globorotalia sp., dorsal view, sample Mf11682. 7—Globorotalia sp., lateral view, sample marine incursion or the development of saline Mf11676. 8—Neogloboquadrina sp., lateral view, sample Mf11676. 9—Neogloboquad- conditions. Additional study is needed to resolve rina sp., ventral view, sample Mf11677. 10—Neogloboquadrina sp., ventral view, sample whether the snails in Mf11684 and therefore Mf11682. 11—Globorotalia sp., lateral view, sample Mf11683. 12—Streptochilus latus, the strontium analysis represent conditions sample Mf11682. 13—Streptochilus latus, apertural view, sample Mf11682. 14—Streptochilus at the site or conditions from another location cf. S. subglobigerum, sample Mf11676. 15—Streptochilus cf. S. subglobigerum, lateral view, where the snail actually lived. If the strontium sample Mf11676. 16—Streptochilus cf. S. subglobigerum, sample Mf11682. 17—Streptochilus datum from the Pyrgulopsis snail is excluded, cf. S. subglobigerum, sample Mf11682. 18—Streptochilus cf. S. subglobigerum, sample the remaining strontium samples were taken at Mf11682. 19—Streptochilus cf. subglobigerum, lateral view, sample Mf11682. 20—Strep- elevations above 70 m asl. tochilus cf. S. subglobigerum, sample Mf11682. 21—Streptochilus latus, lateral view, sample Strontium isotope ratios from the marls and Mf11682. 22—Streptochilus globigerus (Schwager). Santiago Diatomite, San José de Los tufas in the interval between 70 and 120 m asl Cabos, Baja California Sur, México. 23—Streptochilus globigerus (Schwager). Split Moun- elevation in the southern part of the Blythe basin tain Gorge, California. 24—Photomicrograph detail of Streptochilus cf. S. subglobigerum systematically decrease with elevation and then with wall fi nely perforate and fi nely cancellate, sample Mf11682. 25—Photomicrograph increase above 100 m elevation (Fig. 10). Ros- detail of latest chambers of Streptochilus cf. S. subglobigerum with cancelled wall in pen- kowski et al. (2010) attributed this change to tagonal pattern, sample Mf11682. 26—Photomicrograph detail from loop shaped aperture changing 87Sr/86Sr of water inputs into the river in Streptochilus latus, sample Mf11682.

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1234 5 6

789 10 11

12 13 14 15 16 17

18 19 20 21 22 23

1177 24 25 26 10 µm 10 µm 10 µm

Plate 1.

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330 m = highest Bouse Fm containing planktic foraminifers were below sea Lawlor Tuff level, which was at least 25 m above present sea 300 level in the late Miocene and Pliocene (Kominz, 1984; Haq et al., 1987a, 1987b; Johnson et al., 2005; Muller et al., 2008; Miller et al., 2012). Hart Mine A small amount of regional or local uplift Bouse 200 Wash would have been necessary to accommodate a Wash marine incursion and elevate the Bouse Forma- Milpitas Mf11692 Wash Big Maria tion to its current level. A postdepositional uplift Quarry Mf11691 of 500–1000 m was proposed (Metzger, 1968; Smith, 1970; Lucchitta, 1972, 1979; Buising, 100 1990). While this amount of uplift is not consistent with studies that conclude that uplift of the Colorado Plateau occurred in the Eocene, it is consistent with other models that suggest that uplift is ongoing (Karlstrom et al., 2008, 2012; Sea Level 0 Levander et al., 2011).

AGE AND CORRELATION Elevation (m) Mf11679 The presence of Streptochilus latus in sam- –100 ple Mf11682 and the Hart Mine Wash section indicates a late Miocene age between 8.1 and 5.3 Ma (Resig, 1989, 1993). This age is con- ﬁ rmed by the occurrence of Streptochilus cf. –173 m = S. subglobigerum in the lower part of Mf11676

deepest Bouse Fm. Mf11677 –200 and sample Mf11682 that suggests a late Mio- Mf11689 cene age between 10.4 and 7.4 Ma correspond-

Mf11678 ing to planktic foraminiferal zones N16 and

Mf11684 N17 of Blow (1969; as modiﬁ ed and correlated

Mf11676 by Gradstein et al., 2004; Gradstein and Ogg, –300 2005). If the S. subglobigerum identifi cation is 33.00 33.50 34.00 confi rmed with more specimens, the co-occurrence with S. latus constrains the age of the Latitude Bouse Formation in the southern Blythe basin Chara to late Miocene, between 8.1 and 7.4 Ma in the upper half of the late Miocene planktic forami- reworked Cretaceous coccoliths niferal zone N17. If the questioned specimens fresh-water snails are identifi ed as S. globigerus, then the co- occurrence with S. latus would constrain the age Figure 7. Distribution of Chara and reworked Cretaceous coccoliths with respect to eleva- of the Bouse Formation in the southern Blythe tion and latitude in the Blythe basin. The basin contour is modifi ed from Turak (2000), basin to late Miocene, between 5.6 and 5.3 Ma. Spencer et al. (2008), and Pearthree and House (2014). Lithostratigraphic units in the wells At present, the only reliable age for the Bouse are indicated by color: yellow—Bouse Formation; green—limestone, tufa, and marl beds in Formation in the Blythe basin is based on the the Bouse Formation; gray—pre– and post–Bouse Formation units. presence on well-preserved S. latus and is late Miocene, between 8.1 and 5.3 Ma. The late Miocene age based on the planktic Flood deposits are present in northern Mohave elevations of 123 m asl and lower. Planktic fora- foraminifers agrees with the previously reported Valley stratigraphically beneath the Bouse minifers in the Hart Mine Wash section were ages constraining Bouse Formation in the Formation (House et al., 2005a, 2005b, 2008). found at an elevation of 112–123 m asl and cor- Blythe basin. A tuff (9.2 ± 0.3 Ma) and a basalt These deposits were interpreted to record lake relative planktic species in Mf11676 are at ele- (9.6 ± 0.60 Ma) in the underlying Osborne Wash spilling from the north. However, such deposits vations of –106 m bsl. The elevation difference strata of Buising (1988) (Fugro, Inc., 1975, cited have not been found in the Blythe basin, sug- between these assemblages (218–229 m) could in Reynolds et al., 1986; Buising, 1988; Buis- gesting that the arrival of the river was gradual be attributed to faulting and downwarping that ing and Beratan, 1993) suggest that the Bouse and not catastrophic or that the deposits have resulted in differential movement of 300–600 m Formation was deposited after 9.2 Ma. The age not yet been found. The presence or absence of (Metzger et al., 1973). Planktic foraminiferal of the Lawlor Tuff from the upper part of the these deposits is not an indicator of marine or assemblages found at Mf11680 at an elevation of Bouse Formation found at the Buzzards Peak lacustrine deposition. 115 m asl may also be correlative and the eleva- and Amboy localities (Metzger et al., 1973; The portion of the Bouse Formation that con- tion may also be affected by faulting and down- Buising, 1988; Sarna-Wojcicki et al., 2011; tains evidence of marine deposition is today at warping. At the time of deposition, samples Spencer et al., 2013) indicates that deposition

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13 2 14 15 21 17 18 22 3 6 4 5 16 7 10 11 19 23 12 8 1 20

Saline Lakes: Saline Lakes with marine influence: 18. Marmara Sea and Aral Sea, 1. Salt Lake, Hawaii 10. Sabine Lake, Texas and Louisiana 19. Dead Sea Rift Lakes, Isreal 2. Lake Winnipegosis, Canada 11. Lake Ponchtrain, Louisiana 20. Casamance Estuary, Senegal 3. Lake Tecopa, California 12. Bermuda coastal ponds 4. Salton Sea, California 13. Glombak and Hart Vejle, Denmark Estuaries: 5. Estancia Valley, New Mexico 14. Cowpen Marsh, and Tees Marsh, UK 21. Straits of Juan de Fuca, Puget 6. Lacustrine Basins, Spain 15. Salziger and Suesser Sees, Germany Sound, Straits of Georgia 7. Salines playa-lakes, Spain 16. Guadalquivir estuary, Spain 22. San Francisco Bay 8. Lake Qarum, Eygpt 17. Pannonian Lake, Carpathians 23. Gulf of California 9. Saline Lakes, Australia

Figure 8. Location of saline lakes and estuaries considered in analysis. References for lake and estuarine study: 1—Resig (1974); 2—Patterson et al. (1997); Boudreau et al. (2001); 3—Patterson (1987); 4—Arnal (1954, 1958, 1961); 5—Bachhuber and McClellan (1977); 6—Anadon (1989); 7—Giralt et al. (1999); 8—Abu-Zied et al. (2007), Zalat (1995), Flower et al. (2006); 9—Cann and de Deckker (1981); 10—Kane (1967); 11—Otvos (1978); 12— Javaux and Scott (2003); 13—Amsinck et al. (2003); 14—Horton (1999), Horton et al. (1999); 15—Wennrich et al. (2007); 16—Ruiz et al. (2004); 17—Kázmér (1990); 18—Brodsky (1928), Schmalhausen (1950), Boltovskoy and Wright (1976), McHugh et al. (2008), Reidel et al. (2011); 19—Almogi-Labin et al. (1992, 1995); 20—Debenay (1990), Debenay et al. (1994); 21—Cushman and Todd (1947), Cockbain (1963), R.A. Harman (2001, unpublished data); 22—Arnal et al. (1980), Chin et al. (2010); 23—Walton (1955), Bandy (1961). This is a ﬁ le from the Wikimedia Commons (http:// en .wikipedia .org /wiki /File: Mercator _projection _SW .jpg). Imagery is a derivative of National Aeronautics and Space Administration Blue Marble summer month composite with oceans lightened to enhance legibility and contrast. Image created with the Geocart map projection software (by Strebe; http://www .mapthematics .com /ProjectionsList .php ?Projection =181; 5 August 2011).

ended by 4.83 Ma. Both normal and reversed zon and Whitewater sections were assigned to (10.1 ± 0.2 Ma; Peterson, 1975) and overlying magnetic polarity have been noted in the Bouse planktic foraminiferal zones N17–N18 based Painted Hill Formation (6.04 ± 0.18 and 5.94 ± Formation (Kukla, 1976; Malmon et al., 2011). on the occurrence of Globigerinoides obliquus, 0.18 Ma; Matti et al., 1985; Matti and Morton, Preliminary analysis of the Bouse Wash section G. extremus, and Globigerina nepenthes and to 1993). The Imperial Formation exposed in the by Malmon et al. (2011) indicated a paleomag- calcareous nannoplankton zones CN9a–CN10 Garnet Hill section is between 8.0 or 7.6 to netic reversal; unfortunately, there are insufﬁ - based on the occurrence of Discoaster brouweri, 5.32 Ma based on a tephra correlation (Rymer cient data to date this reversal. D. aff. D. surculus, Reticulofenestra pseudo- et al., 1994, 1995) and the presence of Amphiste- Similar ages were reported from the Impe- umbilicata, Sphenolithus abies, and S. neoabies gina gibbosa, which indicates deposition prior rial Formation in the Cabazon, Whitewater, (McDougall et al., 1999; McDougall, 2008a). to the inﬂ ux of sediment derived from the Colo- Garnet Hill, and Fish Creek sections in the These assignments are supported by K/Ar dates rado River (5.32–4.83 Ma; Spencer et al., 2013; Imperial Valley (Fig. 12). Strata in the Caba- from the underlying Coachella Fanglomerate Dorsey et al., 2007, 2011). The older part of the

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TABLE 12. CRITERIA DIFFERENTIATING FORAMINIFERAL ASSEMBLAGES IN SALINE LAKES FROM THOSE IN ESTUARIES Criteria Saline lakes Estuaries Diversity (species/sample) Low; 1–2 species in shallow lakes and <5 in deeper lakes; Low to high exceptions include Salt Lake, Hawaii, and Salton Sea, California Foraminiferal number decreases toward the center of larger lakes Foraminiferal numbers and diversity increase with depth and distance due to the increase in organic carbon content and the decrease from the shoreline in pH of the sediment Composition and distribution Usually dominated by Ammonia, Elphidium, and Quinqueloculina; In low to moderately diverse areas fauna dominated by Ammonia, agglutinated faunas may be common; endemism and isolated Elphidium, and Quinqueloculina; agglutinated faunas are common occurrences if environmental conditions do not promote survival after introduction Aberrant tests Abnormal tests are common Abnormal tests present but not abundant; dwarfed benthic foraminiferal faunas can be found living below sill depth in marine basins in the Gulf of California where low oxygen conditions prevail Planktic foraminifers Absent Rare to common; missing from large areas of the Gulf of California and other estuaries due to rainfall and runoff, and from delta regions where salinity deviates from normal marine Note: Saline lakes and marine estuaries used for this comparison are identiﬁ ed in Figure 8.

S. Blythe Basin N. Blythe Basin Chemehuevi and Mohave-Cottonwood Basins 600 560 m = highest Bouse Fm.

500

400

350 m = 330 m = highest Bouse Fm. highest Lawlor Tuff 300 Bouse Fm.

Hart Mine Osborne Wash Davis Milpitas Bouse Wash 200 Dam Wash Wash Big Maria Topock Quarry Gorge Mf11682 Parker Mf11683 Mf11680 Dam 100 Elevation (m)

Sea Level 0

Pyrgulopsis Mf11679 –100 Sr isotope samples –173 m = O and C isotope samples deepest Bouse Fm. –200 Mf11677 samples with planktic foraminifers Mf11689 microfossil samples Mf11678 Mf11684 –300 Mf11676 33.00 33.50 34.00 34.50 35.00 35.50 North South Latitude

Figure 9. Distribution of isotope and microfossil samples with respect to elevation and latitude. The distribution of planktic foraminifers and the sample with Pyrgulopsis specimen are indicated. The basin contour is modiﬁ ed from Turak (2000), Spencer et al. (2008), and Pearthree and House (2014). Lithostratigraphic units in the wells are indicated by color: yellow—Bouse Formation; green—limestone, tufa, and marl beds in the Bouse Formation; gray—pre– and post–Bouse Formation units.

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Colorado River water (0.71075) youngest Hualapai late Miocene seawater Lake Mead (0.710437) Limestone (0.713654) Cibola Refuge (0.710274) 400

350

330 m = highest Bouse Fm. 300

Elevation (m) 250

200

150 Hart Mf11682 Mine Mf11680 Wash Mf11683100

Sea Level 0

Mf11676 Mf11677 –100 Mf11676 Caliche Barnacle or shell hash Mf11678 Tufa or Marl –173 m = deepest Bouse Fm. Snail –200 0.70900 0.71000 0.71100 Sr ratios

Figure 10. 87Sr/86Sr ratios from caliche, barnacles or shell hash, tufa or marl, and snails present in the Bouse Formation are plotted against elevation. Sr values for the Colorado River water (0.710274 and 0.710437—Gross et al., 2001; 0.71075—Goldstein and Jacobsen, 1988; Spencer and Patchett, 1997) and late Miocene marine water (0.70900) are also plotted. The elevations of samples containing planktic foraminifers are plotted on the left side of the ﬁ gure. Hualapai Limestone Member values range from 0.713654 (youngest) to 0.719536 (oldest) (Roskowski et al., 2010). Trend line for Sr isotopes is from Roskowski et al. (2010).

Imperial Formation exposed in the Fish Creek upper bathyal (150–500 m) before normal sedi- the Bouse Formation in the Yuma basin, the section also contains Amphistegina gibbosa and mentation returned after the megabreccia was Boleo Formation in the Santa Rosalía basin, probably represents the same interval, but does emplaced. The disparity implies a nonconfor- and the Diatomita Santiago Formation in San not contain diagnostic microfossils. mity and that some time is missing. Therefore José de los Cabos, Mexico (Carreño, 1981, Paleomagnetic correlations from the Fish it is possible that the Imperial Formation below 1992). The Bouse Formation in the Yuma Creek section suggest that this section is the megabreccia is at least one chron older than basin occurs primarily in the subsurface and between 6.27 and 5.89 Ma, but also assumes reported by Dorsey et al. (2007, 2011); e.g., contains many of the same species as the that the upper megabreccia was emplaced with either C3An.2n (6.57–6.27 Ma) or C3Bn (7.09– Bouse Formation along the lower Colorado no break in sedimentation. The benthic forami- 6.94 Ma) subchrons. River (Smith, 1970; Olmsted et al., 1973; Win- niferal assemblages indicate that water depths Other sections containing marine sediments terer, 1975): Ammonia beccarii, Elphidium increased from shallow inner neritic (<50 m) to similar in age in the Gulf of California include gunteri, Eoponidella palmerae, and Rosalina

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+2 seawater Milpitas Wash Colpichthys regis Cibola +1

(‰) Parker Buzzards Peak –1 VPDB C 13 δ –2

Limekiln Wash –3

modern –4 Colorado River

Bouse Fm., elevations <100 m –5 Bouse Fm., elevation > 100 m

–16 –14 –12 –10 –8 –6 –4 –2 0 +2

18 δ OVPDB (‰)

Figure 11. δ18O and δ13C values for the Bouse Formation. Isotope values from previous studies by Spencer and Patchett (1996), Poulson and John (2003), and Roskowski et al. (2010) are plotted for the Bouse Formation samples , modern Colorado River water (blue diamonds), and seawater (blue dot). Groups of samples from the same area (Parker, Milpitas Wash, Cibola, and Limekiln Wash) are enclosed by dashed lines. The sample from Buzzards Peak and the samples from the bedding plane where the ﬁ sh Colpichthys regis was found are indicated. VPDB—Vienna Peedee belemnite.

columbiensis. Slides and material are not CONCLUSIONS tions. This dominance suggests a change from available to verify the presence of planktic marine to brackish water such as in a saline foraminifers, and the checklists provided by The foraminiferal associations indicate that lake. Deformed tests compose 1% or less of Winterer (1975) are too vague to make a con- the basal part of the Bouse Formation in the A. beccarii tests in the lower elevations of the fi dent assessment of ages. Blythe basin was marine and that marine sedi- Bouse Formation and suggest marine water. At The most probable age for the Boleo For- ments are found up to elevations of ~123 m an elevation of 123 m and higher, the number mation in the Santa Rosalia basin, Baja Cali- asl (Fig. 13). Above this elevation, the limited of deformed tests in the A. beccarii population fornia Norte, is late Miocene and ranges from fauna (a single benthic foraminiferal species) increases and can include as much as 5% of the 7.09 to 6.93 Ma (Geomagnetic Polarity Time coupled with the absence of planktic species population. These higher values suggest salini- Scale subchron C3Bn) for the base and 6.27– indicates that the marine water is replaced by ties differ from normal marine, but more data 6.14 Ma for the top of the formation (Holt saline lake water. Chara, a green algae found in are needed to develop this line of evidence. et al., 2000). Foraminiferal assemblages from fresh to slightly brackish water, fi rst appears at Arguments in favor of a lacustrine origin of the Boleo Formation (A. Miranda, personal 85 m asl but becomes more common at eleva- the Bouse Formation are based on the presence data) contain a diverse assemblage including tions of 110 m and higher, and reworked Creta- of a saline lake, avian transport of foraminiferal Amphistegina gibbosa and could be correla- ceous cocco liths from the Mancos Shale appear species, isotopes, no evidence of uplift, and a tive with the Imperial Formation found in the at ~110 m asl and higher. The dominance of variety of sedimentological arguments such as White water, Cabazon, and Garnet Hill sections. Ammonia beccarii is low throughout the lower fl ood deposits and the presence of Colorado The assemblages are more diverse than those part of the Bouse Formation, but it becomes River–derived sediments. Faunal composition found in the Bouse Formation, but contain the dominant (or only) foraminiferal species (benthic foraminiferal assemblages and the many of the same species. between 110–126 m asl and higher eleva- presence or absence of planktic foraminifers),

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17, 25 Basin (marine)

9.6 Ma Metzger et al. (1973); 8—Ingle (1973, Metzger Blythe Gravel Osborne 9.2 and Bouse Fm. Bouse ? 7, 10, 11, 7, 10, 11, Lawlor Tuff (4.83 Ma) CO. River 1, 2, 3, 4, 6, * * d in Dorsey et al. (2007, 2011). References References d in Dorsey et al. (2007, 2011). 95); 21—Winker and Kidwell (1996); 22— 95); 21—Winker tions used for units: OF—Ocotillo formation; tions used for Qa Split Area Palm Impact Carrizo Group Imperial Springs

13, 14, 23 Mountain Formation Formation

ernative Split Mountain Gorge–Fish Creek column ernative Split Mountain Gorge–Fish Creek sed for each section are discussed in the text. Marine each section are sed for Coyote Mts. Palm Springs Group Springs Palm McDougall (2008b) and coastal onlap curves from re LMB 26 Qa UMB Split 2.4 Ma Cane- brake Cong.

Split Mt. Mountain Gorge - 14, 15, 21, 23, 24, 25, Formation

Lcyium Mbr. Imperial Fm. Alternative Fish Creek 5, 8, 12, 13, Olla and Arroyo Diablo Fm. Palm Springs Group Springs Palm 26 LMB Qa UMB Split 2.4 Ma Imperial Cane- brake Cong. Split Mt. Mountain Formation Gorge - 14, 15, 21, Formation 23, 24, 25, Lcyium Mbr. Fish Creek 5, 8, 12, 13, Olla and Arroyo Diablo Fm. ? ? Hill ? Garnet 7.6-8.0 Ma

? 19, 20, 25

Imperial Fm. * 10.1Ma Fgl.

* * Coachella Qa 6.0 Ma 22, 25 water White- 9,16, 18, Formation Imperial Fm. Painted Hill

Qa Fgl. 22, 25 Fm. Cabazon Cabazon Hathaway Formation Formation Painted Hill Imperial qullah et al. (1980); 12—Johnson et al. (1983); 13—Quinn and Cronin (1984); 14—Winker (1987); 15—Dean (1988, (1984); 14—Winker qullah et al. (1980); 12—Johnson (1983); 13—Quinn and Cronin Hallian Benthic Mohnian Venturian Repettian Delmontian Wheelerian Foraminiferal N15 N17 N16 N18 N22 N17a N20/21 Stages and Zones Planktic CN9 CN8 CN6 CN7 Bukry 1975) CN10 CN12 CN11 CN14 CN13 (1973, CN15 Zones alt. Calcareous NN8

NN9 NN11 (1971) Martini NN11 NN21 NN13 NN20 NN18 NN12 NN10 NN15 NN17 NN19 NN14 NN16

Nannoplankton Late

L E E M

Epoch

Pliocene Pleist. Miocene

Polarity Chrons

C5 C1 C3 C4 C2 C2A C4A C3B C3A Time (Ma) Time 4 1 2 3 5 6 7 8 9 11 10 McDougall et al. (1999); 23—Cassiliano (2002); 24—Dorsey et al. (2007); 25—McDougall (2008a); 26—Dorsey et al. (2011). McDougall et al. (1999); 23—Cassiliano (2002); 24—Dorsey (2007); 25—McDougall (2008a); 26—Dorsey (2011). Abbrevia Figure 12. Correlation of sections in the Salton Trough and along the lower Colorado (CO.) River. Interpretations of the data u Interpretations Colorado (CO.) River. and along the lower Trough of sections in the Salton 12. Correlation Figure of stages and zones a scale and correlation Time shaded. marginal marine units are white; continental, lacustrine, or units are The alt et al. (2008). Pleist—Pleistocene. Kominz (1984), Haq et al. (1987a, 1987b), Johnson (2005), and Muller from are (1968); 4—Smith (1970); 5—Stump (1972); 6—Olmsted et al. (1973); 7— the sections: 1—Smith (1960); 2—Damon (1965); 3—Metzger for (1975); 11—Shaﬁ 1974); 9—Peterson (1975); 10—Winterer et al. (1994, 1995); 20—Powell (19 1990, 1996); 16—Matti et al. (1985); 17—Buising (1990); 18—Matti and Morton (1993); 19—Rymer Qa—Quaternary alluvium. megabreccia; Gypsum; Fcgl, fgl—fanglomerate; LMB—lower BF—Brawley Formation; FCG—Fish Creek assumes that the unconformity observed with the emplacement of the upper megabreccia (UMB) was of a longer duration than assume (UMB) was of a longer megabreccia assumes that the unconformity observed with emplacement of upper

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300 Lawlor Tuff (4.83 Ma) 330 m = highest Bouse Fm. Hart Mine Osborne Wash Bouse 200 Milpitas Big Maria Wash Wash Wash Quarry Mf11682 100 Mf11683 Mf11680 ? ?

Sea Level 0 Elevation (m)

–100 Mf11679

–200 –173 m = deepest Bouse Fm. Mf11677 Mf11689 Mf11678

–300 Mf11684 Mf11676 33.00 33.50 34.00 Latitude

lowest monospecific benthic foraminiferal diversity; Bouse Formation highest occurrence inner neritic biofacies

highest occurrence of planktic foraminifers Pre and post-Bouse units lowest occurrence of Chara lowest occurrence of reworked Cretaceous coccoliths Basin contour (Turak, 2000) freshwater snails

Figure 13. Summary of biostratigraphic events that occur in the transition from marine to saline lake conditions in the Bouse Formation of the Blythe basin. Dashed lines indicate the highest or lowest occurrence of an event. The presence of freshwater snails in the northern Blythe basin prior to marine faunas is noted. The snails reappear again in the northern part of the basin at higher elevations after transition from marine to saline lake. Lithostrati- graphic units in the wells are indicated by color: yellow—Bouse Formation; green—limestone, tufa, and marl beds in the Bouse Formation; gray—pre– and post–Bouse Formation units. The basin contour is modiﬁ ed from Turak (2000), Spencer et al. (2008), and Pearthree and House (2014).

and characteristics (abundance and deformity part of the Blythe basin near Cibola have a ACKNOWLEDGMENTS of A. beccarii) of the Bouse assemblages sug- marine signal. Perhaps with additional study of We thank Elizabeth Mennow at the U.S. Geologi- gest that deposition was initially in a marine the Sr sources and concentration, and more iso- cal Survey Flagstaff Micropaleontology Laboratory estuary and that a saline lake developed when tope analysis, a marine signal will be detected for her work and assistance in preparing and locating the sediments now found at elevations between in the isotopes from the lower part of the Bouse samples and Debra Block for assisting with geographic 110–123 m and higher were deposited. Salinity Formation. Although no evidence of uplift was information system work. We also thank Kyle House models (Spencer and Patchett, 1997; Spencer observed, when differential movement due to and Sue Beard for listening and discussing various ideas, and for encouragement, and Yolanda Hornelas et al., 2013) that assume the Blythe basin was a faults and downwarping is accounted for, the Orozco, in Laboratorio de Microscopía Electrónica de lake ﬁ lled by Colorado River water indicate that marine portion of the Bouse Formation may Barrido, Instituto de Ciencias del Mar y Limnología, initially salinities were highly variable, ranging be found to be below late Miocene sea level. Universidad Nacional Autónoma de México (UNAM), from fresh to hyposaline, and did not approxi- Reworked Cretaceous microfossils, which are for taking scanning electron microscope photomicro- graphs. We appreciate the reviews and comments pro- mate marine salinities until just before spillover often used as evidence of Colorado River sedi- vided by Keith Howard and Charles Powell II of the of the lake. The isotopic data are interpreted as ments, are present in the Bouse Formation at U.S. Geological Survey, and Andy Cohen of the Uni- indicating lacustrine deposition, and since most elevations of 110 m and higher. versity of Arizona. Miranda appreciates the ﬁ nancial of the isotope samples are from the upper por- Planktic foraminifers indicate a late Miocene support provided by PAPIIT (Programa de Apoyo a tion of the Bouse Formation, this is expected. age between 8.1 and 5.3 Ma for the oldest part of Proyectos de Investigación e Innovación Tecnológica) UNAM (IN102211 to A.L. Carreño) and CONACYT Strontium isotope samples from elevations of the Bouse Formation in the southern part of the (Consejo Nacional de Ciencia y Tecnología, scholar- 70–123 m decrease from the high Colorado Blythe basin. This age is between ages derived ship 172854). River values, indicating that some mixing of from other sources that limit the age of the Bouse different water masses occurred. Values increase Formation to younger than 9.2 Ma and no older REFERENCES CITED above this and remain high. Oxygen and carbon than 4.83 Ma in the Blythe basin. Benthic and Abu-Zied, R.H., Keatings, K.W., and Flower, R.J., 2007, isotopes were also sampled primarily from the planktic foraminifers that correlate with other Environmental controls on foraminifera in Lake Qarun, saline lake portion of the formation and indicate late Miocene foraminiferal assemblages suggest Egypt: Journal of Foraminiferal Research, v. 37, p. 136–149, doi: 10 .2113 /gsjfr .37 .2 .136 . a continental source. Samples from the lowest that the Bouse Formation was deposited at the Aguirre, J., Riding, R., and Braga, J.C., 2000, Diversity of elevations (~80–90 m) and from the southern northern end of the proto–Gulf of California. coralline red algae: Origination and extinction patterns

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from the Early Cretaceous to the Pleistocene: Paleo- Bradshaw, J.S., 1961, Laboratory experiments on the ecol- Crabtree, C.B., 1989, A new silverside of the genus Col- biology, v. 26, p. 651–667, doi: 10 .1666 /0094 -8373 ogy of foraminifera: Contributions from the Cush- pichthys (Atheriniformes:Atherinidae) from the Gulf (2000)026 <0651: DOCRAO>2.0 .CO;2. man Foundation for Foraminiferal Research, v. 12, of California, Mexico: Copeia, v. 1989, p. 558–568. Almogi-Labin, A., Perelis-Grossovicz, L., and Raab, M., p. 87–106. Crossey, L.J., Karlstrom, K.E., Dorsey, R.J., and Pearce, 1992, Living Ammonia from a hypersaline inland Brodsky, A.A., 1928, Foraminifera (Polythalamia) in wells J.L., 2013, Geochemistry of springs, travertines and pool, Dead Sea area, Israel: Journal of Foraminiferal of the Kara-Kum Desert: Trudy Sredne-Aziatskogo lacustrine carbonates of the Grand Canyon region Research, v. 22, p. 257–266, doi: 10 .2113 /gsjfr .22 .3 Gosudarstvennogo Universiteta, ser. 8a, Zoologija, over the past 12 million years: The importance of .257 . v. 8, p. 6–36 (in Russian). groundwater in initiating downward integration of the Almogi-Labin, A., Siman-Tov, R., Roenfeld, A., and Debard, Bronnimann, P., and Resig, J.M., 1971, A Neogene globi- Colorado River system: Geological Society of America E., 1995, Occurrence and distribution of the foramini- gerinacean biochronologic timescale of the south- Abstracts with Programs, v. 45, no. 7, p. 252. fer Ammonia beccarii tepida (Cushman) in water bod- western Pacifi c, in Winterer, E.L., Initial reports of the Culver, S.J., and Buzas, M.A., 1986, Distribution of recent ies, recent and Quaternary, of the Dead Sea rift, Israel: Deep Sea Drilling Project, Leg 7: Washington, D.C., benthic foraminifera off the North American Pacifi c Marine Micropaleontology, v. 26, p. 153–159, doi: 10 U.S. Government Printing Offi ce, p 1235–1469, doi:10 coast from California to Baja: Smithsonian Contribu- .1016 /0377 -8398 (95)00013-5 . .2973 /dsdp .proc .7 .128 .1971 . tions to the Marine Sciences 28, 634 p. Amsinck, S.L., Jeppesen, E., and Ryves, D., 2003, Cladoceran Buising, A.V., 1988, Depositional and tectonic evolution of Cushman, J.A., 1923, The foraminifera of the Atlantic stratigraphy in two shallow brackish lakes with special the northern proto-Gulf of California and Lower Colo- Ocean, Part IV—Lagenidae: U.S. National Museum reference to changes in salinity, macrophyte abundance rado River, as documented in the Mio-Pliocene Bouse Bulletin 104, 228 p. and fi sh predation: Journal of Paleolimnology, v. 29, formation and bracketing units, southeastern Califor- Cushman, J.A., 1925, Recent foraminifera from British p. 495–507, doi: 10 .1023 /A: 1024470329314 . nia and western Arizona [Ph.D. thesis]: Santa Barbara, Columbia: Contributions from the Cushman Labora- Anadon, P., 1989, Los lagos salinos interiores (atalasicos) University of California, 196 p. tory for Foraminiferal Research, v. 1, p. 38–47. con faunas de afi nidad marina del Cenozoico de la Buising, A.V., 1990, The Bouse Formation and bracketing Cushman, J.A., and Todd, R., 1947, Foraminifera from the Península Ibérica: Acta Geologica Hispanica, v. 24, units, southeastern California and western Arizona: coast of Washington: Cushman Laboratory for Forami- p. 83–102. Implications for the evolution of the proto–Gulf of Cal- niferal Research Special Publication 21, 23 p. Arnal, R.E., 1954, Preliminary report on the sediments and ifornia and the lower Colorado River: Journal of Geo- Cushman, J.A., and Wickenden, R.T.D., 1929, Recent foraminifera from the Salton Sea, southern California physical Research, v. 95, no. B12, p. 20,111–20,132, foraminifera from off Juan Fernandez Islands: U.S. [abs.]: Geological Society of America Bulletin, v. 65, doi: 10 .1029 /JB095iB12p20111 . National Museum Proceedings, no. 2780, v. 75, p. 1227–1228. Buising, A.V., 1993, Stratigraphic overview of the Bouse For- p. 1–16. Arnal, R.E., 1955, Some occurrences of abnormal forami- mation and gravels of the Colorado River, in Sherrod, Damon, P.E., 1965, Summary of research accomplishments, nifera: Sigma Gamma Epsilon Compass, v. 32, no. 3, D.R., and Nielson, J.E., eds., Tertiary stratigraphy of in Damon, P.E., ed., Correlation and Chronology of p. 185–194. highly extended areas, California, Arizona, and Nevada: Ore Deposits and Volcanic Rocks: U.S. Atomic Energy Arnal, R.E., 1958, Rhizapoda from the Salton Sea, Califor- U.S. Geological Survey Bulletin 2053, p. 159–163. Committee Annual Progress Report C00–689–50, nia: Contributions from the Cushman Foundation for Buising, A.V., and Beratan, K.K., 1993, Preliminary strati- p. 5–60. Foraminiferal Research, v. 9, p. 36–45. graphic reevaluation of upper Tertiary units, Osborne Darling, K., Thomas, E., Kasemann, S., Smart, C.W., Seears , Arnal, R.E., 1961, Limnology, sedimentation, and micro- Wash area, La Paz County, Arizona, in Sherrod, D.R., H., and Wade, C., 2009, Evolution from benthos to organisms of the Salton Sea, California: Geological and Nielson, J.E., eds., Tertiary stratigraphy of highly plankton: Rare or common?: Geological Society of Society of America Bulletin, v. 72, p. 427–478, doi: 10 extended areas, California, Arizona, and Nevada: U.S. America Abstracts with Programs, v. 40, no. 6, p. 204. .1130 /0016 -7606 (1961)72[427: LSAMOT]2 .0 .CO;2 . Geological Survey Bulletin 2053, p. 159–163. Dean, M.A., 1988, Genesis, mineralogy, and stratigraphy of Arnal, R.E., Quinterno, P.J., Conomos, T.J., and Gram, R., Buzas, M.A., and Culver, S.J., 1990, Recent benthic forami- the Neogene Fish Creek Gypsum, southwestern Salton 1980, Trends in the distribution of recent foramin- niferal provinces on the Pacifi c continental margin of Trough, California [M.S. thesis]: San Diego, Califor- ifera in San Francisco Bay, in Sliter, W.V., ed., Stud- North and Central America: Journal of Foraminiferal nia, San Diego State University, 150 p. ies in marine micropaleontology and paleoecology: A Research, v. 20, p. 326–335, doi: 10 .2113 /gsjfr .20 .4 Dean, M.A., 1990, The Neogene Fish Creek Gypsum; memorial volume to Orville L. Bandy: Cushman Foun- .326 . forerunner to the incursion of the Gulf of California dation for Foraminiferal Research Special Publication Burne, R.V., Bauld, J., and de Deckker, P., 1980, Saline lake into the western Salton Trough: Geological Society of 19, p. 17–39. charophytes and their geological signifi cance: Journal America Abstracts with Programs, v. 22, no. 3, p. 18. Bachhuber, F.W., and McClellan, W.A., 1977, Paleoecology of Sedimentary Petrology, v. 50, p. 281–293, doi: 10 Dean, M.A., 1996, Neogene Fish Creek Gypsum and associ- of marine foraminifera in the pluvial Estancia Val- .1306 /212F79D2 -2B24 -11D7 -8648000102C1865D . ated stratigraphy and paleontology, southwestern Salton ley, central New Mexico: Quaternary Research, v. 7, Cann, J.H., and de Deckker, P., 1981, Fossil Quaternary and Trough, California, in Abbott, P.L., and Seymour, D.C., p. 254–267, doi: 10 .1016 /0033 -5894 (77)90040 -0 . living foraminifera from athalassic (non-marine) saline eds., Sturzstroms and detachment faults, Anza-Borrego Bandy, O.L., 1961, Distribution of foraminifera, radiolaria lakes, southern Australia: Journal of Paleontology, Desert State Park, California: Santa Ana, California, and diatoms in sediments of the Gulf of California: v. 55, p. 660–670. South Coast Geological Society, p. 123–148. Micropaleontology, v. 7, p. 1–26, doi: 10 .2307 /1484140 . Carreño, A.L., 1981, Ostrácodos y foraminíferos planctóni- Debenay, J.-P., 1990, Recent foraminiferal assemblages and Be, A.W.H., and Tolderlund, D.S., 1971, Distribution and cos de la localidad Loma del Tirabuzón, Santa Rosalía, their distribution related to environmental stress in the ecology of living planktonic foraminifera in surface Baja California Sur, e implicaciones bioestratigráfi - paralic environments of West Africa (Cape Timitis to waters of the Atlantic and Indian oceans, in Funnell, cas y paleoecológicas: Revista Mexicana de Ciencias Ebrie Lagoon): Journal of Foraminiferal Research, B.M., and Riedel, W.R., eds., The micropaleontology Geológicas, v. 5, p. 55–64. v. 20, p. 267–282, doi: 10 .2113 /gsjfr .20 .3 .267 . of oceans: Cambridge, UK, Cambridge University Carreño, A.L., 1992, Neogene microfossils from the Debenay, J.-P., Pages, J., and Guillou, J.-J., 1994, Transfor- Press, p. 105–149. Santi ago Diatomite, Baja California Sur, Mexico, in mation of a subtropical river into a hyperhaline estuary: Bermudez, P.J., 1949, Tertiary smaller foraminifera of Alcayde-Orraca, M., and Gómez-Caballero, A., eds., The Casamance River (Senegal)—Paleogeographical the Dominican Republic: Cushman Laboratory for Calcareous Neogene microfossils of Baja California implications: Palaeogeography, Palaeoclimatology, Forami niferal Research Special Publication 25, 322 p. Sur, México: Paleontología Mexicana, v. 39, no. 2, Palaeoecology, v. 107, p. 103–119, doi: 10 .1016 /0031 Bijma, J., Faber, W.W., Jr., and Hemleben, C., 1990, Tem- p. 34–93. -0182 (94)90167 -8 . perature and salinity limits for growth and survival of Carr, W.J., and Dickey, D.D., 1980, Geological map of the Debenay, J.-P., Beneteau, E., Zhang, J., Stouff, V., Geslin, E., some planktonic foraminifers in laboratory cultures: Vidal California and Parker, SW, California-Arizona Redois, F., and Fernandes-Gonzalez, M., 1998, Ammo- Journal of Foraminiferal Research, v. 20, p. 95–116, quadrangles: U.S. Geological Survey Miscellaneous nia beccarii and Ammonia tepida (Foraminifera): Mor- doi: 10 .2113 /gsjfr .20 .2 .95 . Investigations Series Map I-1125, scale: 1:24,000. phofunctional arguments for their distinction: Marine Blow, W.H., 1969, Late middle Eocene to recent planktic Cassiliano, M.L., 2002, Revision of the stratigraphic nomen- Micropaleontology, v. 34, p. 235–244, doi: 10 .1016 foraminiferal biostratigraphy, in Brönnimann, P., and clature of the Plio-Pleistocene Palm Spring Group /S0377 -8398 (98)00010 -3 . Renz, H.H., eds., Proceedings of the First International (new rank), Anza Borrego Desert, southern California: Debenay, J.-P., Geslin, E., Eichler, B.B., Duleba, W., Syl- Conference on Planktonic Microfossils, 1967, Volume San Diego Society of Natural History Proceedings, vestre, F., and Eichler, P., 2001, Foraminiferal assem- 1: Leiden, E.J. Brill, p. 199–422. v. 38, 30 p., scale 1:30,000. blages in a hypersaline lagoon, Araruama (R.J.) Brazil: Boltovskoy, E., and Wright, R., 1976, Recent foraminifera: Chin, J.L., Woodrow, D.L., McGann, M., Wong, F.L., Journal of Foraminiferal Research, v. 31, p. 133–151, The Hague, W. Junk, 515 p. Fregoso, T., and Jaffe, B.E., 2010, Estuarine sedimen- doi: 10 .2113 /0310133 . Boudreau, R.E.A., Patterson, R.T., Dalby, A.P., and tation, sediment character, and foraminiferal distribu- De Klasz, I., Kroon, D., and van Hinte, J.E., 1989, Notes on McKillop , W.B., 2001, Non-marine occurrence of tion in central San Francisco Bay, California: U.S. the foraminiferal genera Laterostomella de Klasz and the foraminifera Cribroelphidium gunteri in northern Geological Survey Open-File Report 2010–1130, 58 p. Rerat and Streptochilus Bronnimann and Resig, 1989: Lake Winnipegosis, Manitoba, Canada: Journal of Cockbain, A.E., 1963, Distribution of foraminifera in Juan Journal of Micropalaeontology, v. 8, p. 215–225, doi: Forami niferal Research, v. 31, p. 108–119, doi: 10 .2113 de Fuca and Georgia Straits, British Columbia, Can- 10 .1144 /jm .8 .2 .215 . /0310108. ada: Contributions from the Cushman Foundation for DeLaca, T.E., and Lipps, J.H., 1972, The mechanism and Bradshaw, J.S., 1957, Laboratory studies on the rate of Foraminiferal Research, v. 14, p. 37–57. adaptive signifi cance of attachment and substrate pitting growth of the foraminifer, “Streblus beccarii (Linne) Cole, W.S., 1931, The Pliocene and Pleistocene foraminifera in the foraminiferan Rosalina globularis d’Orbigny: var tepida (Cushman): Journal of Paleontology, v. 31, of Florida: Florida State Geological Survey Bulletin 6, Journal of Foraminiferal Research, v. 2, p. 68–72, doi: p. 1138–1147. 79 p. 10 .2113 /gsjfr .2 .2 .68

866 Geosphere, October 2014

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/5/842/3333907/842.pdf by guest on 26 September 2021 Marine incursion, Colorado River corridor

Dobson, M., and Haynes, J., 1973, Association of foraminif- Hammer, U.T., 1986, Saline lake ecosystems of the world: Cushman Foundation for Foraminiferal Research Spe- era with hydroids on the deep shelf: Micropaleontol- Dordrecht, W. Junk Publishers, 616 p. cial Publication 19, p. 163–195. ogy, v. 19, p. 78–90, doi: 10 .2307 /1484966 . Haq, B.U., Hardenbol, J., and Vail, P.R., 1987a, Chronol- Ingle, J.C., Jr., and Keller, G., 1980, Benthic foraminiferal Dorsey, R.J., Fluette, A., McDougall, K., Housen, B.A., ogy of fl uctuating sea levels since the Triassic: Sci- biofacies of western Pacifi c margin between 40°S and Janecke, S.U., Axen, G.J., and Shirvell, C.R., 2007, ence, v. 235, p. 1156–1167, doi: 10 .1126 /science .235 32°N, in Field, M.E., et al., eds., Quaternary deposi- Chronology of Miocene–Pliocene deposits at Split .4793 .1156 . tional environments of the Pacifi c Coast: Pacifi c Coast Mountain Gorge, southern California: A record of Haq, B.U., Hardenbol, J., and Vail, P.R., 1987b, The new Paleogeography Symposium 4: Los Angeles, Califor- regional tectonics and Colorado River evolution: Geol- chronostratigraphic basis of Cenozoic and Mesozoic nia, Pacifi c Section, Society of Economic Paleontolo- ogy, v. 35, p. 57–60, doi: 10 .1130 /G23139A .1 . sea level cycles, in Ross, C.A., and Harman, D., eds., gists and Mineralogist, p. 341–355. Dorsey, R.J., Housen, B.A., Janecke, S.U., Fanning, C.M., Time and depositional history of eustatic sequences— Israelsky, M.C., 1949, Oscillation chart: American Associa- and Spears, A.L.F., 2011, Stratigraphic record of basin Constraints on seismic stratigraphy: Cushman Founda- tion of Petroleum Geologists Bulletin, v. 33, p. 92–98. development within the San Andreas fault system: Late tion for Foraminiferal Research Special Publication 24, Javaux, E.J., and Scott, D.B., 2003, Illustration of modern Cenozoic Fish Creek–Vallecito basin, southern Cali- p. 7–13. benthic foraminifera from Bermuda and remarks on fornia: Geological Society of America Bulletin, v. 123, Hayward, B.W., Buzas, M.A., Buzas-Stephens, P., and Holz- distribution in other subtropical/tropical area: Paleon- p. 771–793, doi: 10 .1130 /B30168 .1 . mann, M., 2003, The lost types of Rotalia beccarii tologia Electronica v. 6, no.4, 296 p. Douglas, R.G., 1979, Benthic foraminiferal ecology and var. tepida Cushman 1926: Journal of Foraminiferal Johnson, C., Bloch, R.B., and Graham, S.A., 2005, Tertiary paleoecology: A review of concepts and methods, in Research, v. 33, p. 352–354, doi: 10 .2113 /0330352 . sequences of the central San Joaquin Basin, Califor- Lipps, J.H., et al., eds., Foraminiferal ecology and Hayward, B.W., Holzmann, M., Grenfell, H.R., Pawlowski, nia: Age control and eustatic versus tectonic forcing paleoecology: Society of Economic Paleontologists J., and Triggs, C.M., 2004, Morphological distinction factors: Pacific Section, American Association of and Mineralogists Short Course Notes 6, p. 21–61, doi: of molecular types in Ammonia—Towards a taxonomic Petroleum Geologists Miscellaneous Publication 49, 10 .2110 /scn .79 .06 .0021 . revision of the world’s most commonly misidenti- 1 sheet. Douglas, R.G., and Heitman, H.L., 1979, Slope and basin fi ed foraminifera: Marine Micropaleontology, v. 50, Johnson, N.M., Offi cer, C.B., Opdyke, N.D., Woodard, benthic foraminifera of the California borderland, in p. 237–271, doi: 10 .1016 /S0377-8398 (03)00074 -4 . G.D., Zeitler, P.K., and Lindsay, E.H., 1983, Rates of Doyle, L.J., and Pilkey, O.H., eds., Geology of conti- Hemleben, C., Spindler, M., and Anderson, O.R., 1989, late Cenozoic tectonism in the Vallecito–Fish Creek nental slopes: Society of Economic Paleontologists and Modern planktonic foraminifera: New York, Springer- basin, western Imperial Valley, California: Geology, Mineralogists Special Publication 27, p. 231–246, doi: Verlag, 363 p. v. 11, p. 664–667, doi: 10 .1130 /0091 -7613 (1983)11 10 .2110 /pec .79 .27 .0231 . Hershler, R., 1994, A review of the North American fresh- <664: ROLCTI>2 .0 .CO;2 . Durham, J.W., and Allison, E.C., 1960, Part I. Geologic his- water snail genus Pyrgulopsis (hydrobiidae): Smithso- Karlstrom, K.E., Crow, R.S., Crossey, L.J., Coblentz, D.J., tory: The geologic history of Baja California and its nian Contributions to Zoology 554, 115 p. and Van Wijk, W., 2008, Model for tectonically driven marine faunas, in Symposium on the biogeography of Holt, J.W., Holt, E.W., and Stock, J.M., 2000, An age con- incision of the younger than 6 Ma Grand Canyon: Baja California and adjacent seas: Systematic Zoology, straint on Gulf of California rifting from the Santa Geology, v. 36, p. 835–838, doi: 10 .1130 /G25032A .1 . v. 9, no. 2, p. 47–91, doi: 10 .2307 /2411859 . Rosalia basin, Baja, California Sur, Mexico: Geologi- Karlstrom, K.E., et al., 2012, Mantle-driven dynamic uplift Ehrenberg, C.G., 1843, Verbreitung und Einfl uss des mikro- cal Society of America Bulletin, v. 112, p. 540–549, of the Rocky Mountains and Colorado Plateau and its skopischen Lebens in Sud- und Nord-Americka: doi: 10 .1130 /0016 -7606 (2000)112 <540: AACOGO>2 surface response: Toward a unifi ed hypothesis: Litho- Konigliche Akademie der Wissenschaften zur Berlin, .0 .CO;2 . sphere, v. 4, p. 3–22, doi: 10 .1130 /L150 .1 . Abhandlungen, 157 p. Horton, B.P., 1999, The distribution of contemporary inter- Kane, H.E., 1967, Recent microfaunal biofacies in Sabine Ellison, R.L., and Nichols, M.M., 1970, Estuarine foraminif- tidal foraminifera at Cowpen March, Tees estuary, Lake and environs, Texas and Louisiana: Journal of era from the Rappahannock River, Virginia: Contribu- UK: Implications for studies of Holocene sea-level Paleontology, v. 41, p. 947–964. tions from the Cushman Foundation of Foraminiferal changes: Palaeogeography, Palaeoclimatology, Palaeo- Kázmér, M., 1990, Birth, life and death of the Pannonian Research, v. 21, no. 1, p. 1–17. ecology, v. 149, p. 127–149, doi: 10 .1016 /S0031 -0182 Lake: Palaeogeography, Palaeoclimatology, Palaeo- Finger, K.L., 1990, Atlas of California Neogene foraminif- (98)00197 -7 . ecology, v. 79, p. 171–188, doi:10 .1016 /0031 -0182 era: Cushman Foundation for Foraminiferal Research Horton, B.P., Edwards, R.J., and Lloyd, J.M., 1999, UK (90)90111 -J . Special Publication 28, 271 p. intertidal foraminiferal distributions: Implications for Kennett, J.P., and Srinivasan, M.S., 1983, Neogene plank- Flower, R.J., Stickley, C., Rose, N., Peglar, S., Fathi, A.A., sea-level studies: Marine Micropaleontology, v. 36, tonic foraminifera; a phylogenetic atlas: Stroudsburg, and Appleby, P.G., 2006, Environmental change at the p. 205–223, doi: 10 .1016 /S0377 -8398 (99)00003 -1 . Pennsylvania, Hutchinson Ross, 265 p. desert margin: An assessment of recent palaeolimno- House, P.K., Pearthree, P.A., and Perkins, M.E., 2005a, Kominz, M.A., 1984, Oceanic ridge volumes and sea level logical records in Lake Qarun middle Egypt: Journal Tephrochronologic and stratigraphic constraints on change—An error analysis, in Schlee, J., ed., Interre- of Paleolimnology, v. 35, p. 1–24, doi: 10 .1007 /s10933 the inception and early evolution of the lower Colo- gional unconformities and hydrocarbon accumulation: -005 -6393 -2 . rado River support lacustrine overfl ow as the principal American Association of Petroleum Geologists Mem- Fugro, Inc., 1975, Geotechnical investigations, Parker Valley formative mechanism: Geological Society of America oir 36, p. 109–127. alternate site, Sun Desert Nuclear Project: San Diego, Abstracts with Programs, v. 37, no. 7, p. 110. Kukla, G.J., 1976, Preliminary report on magnetostrati- California, San Diego Gas and Electric Company, sec- House, P.K., Pearthree, P.A., Howard, K.A., Bell, J.W., Per- graphic study of sediments near Blythe, California and tion 2.5, p. 53–63. kins, M.E., Faulds, J.E., and Brock, A.L., 2005b, Birth Parker Valley, Arizona: San Diego Gas and Electric Galloway, J.J., and Wissler, S.G., 1927, Pleistocene forami- of the lower Colorado River—Stratigraphic and geo- Company, Early Site Review, Sundesert Nuclear Proj- nifera from the Lomita Quarry, Palos Verdes Hills, morphic evidence for its inception near the conjunc- ect, Appendix 2.5B, p. 186–191. California: Journal of Paleontology, v. 1, no. 3, tion of Nevada, Arizona, and California, in Pederson, Langer, M.R., 1993, Epiphytic foraminifera: Marine Micro- p. 35–87. J., and Dehler, C.M., eds., Interior western United paleontology, v. 20, p. 235–265, doi:10 .1016 /0377 Giralt, S., Burjachs, F., Roca, J.R., and Julia, R., 1999, Late States: Geological Society of America Field Guide 6, -8398 (93)90035 -V . Glacial to early Holocene environmental adjustment in p. 357–387, doi: 10 .1130 /2005 .fl d006 (17) . Lankford, R.R., and Phleger, F.B., 1973, Foraminifera from the Mediterranean semi-arid zone of the Salines playa- House, P.K., Pearthree, P.A., and Perkins, M.E., 2008, the nearshore turbulent zone, western North America: lake (Alacante, Spain): Journal of Paleolimnology, Stratigraphic evidence for the role of lake spillover in Journal of Foraminiferal Research, v. 3, p. 101–132, v. 21, p. 449–460, doi: 10 .1023 /A: 1008000513938 . the inception of the lower Colorado River in southern doi: 10 .2113 /gsjfr .3 .3 .101 . Goldstein, S.J., and Jacobsen, S.B., 1988, Nd and Sr iso- Nevada and western Arizona, in Reheis, M.C., et al., Le Cadre, V., Debenay, J.-P., and Lesourd, M., 2003, Low topic systematics of river water suspended material: eds., Late Cenozoic drainage history of the southwest- pH effects on Ammonia beccarii test deformation: Implications for crustal evolution: Earth and Planetary ern Great Basin and lower Colorado River region: Geo- Implications for using test deformations as a pollution Science Letters, v. 87, p. 249–265, doi: 10 .1016 /0012 logic and biotic perspectives: Geological Society of indicator: Journal of Foraminiferal Research, v. 33, -821X (88)90013 -1 . America Special Paper 439, p. 335–353, doi:10 .1130 p. 1–9, doi: 10 .2113 /0330001 . Gradstein, F.M., and Ogg, J.G., 2005, Time scale, in Selley, /2008 .2439 (15) . Lee, K.E., Kimoto, K., and Kim, D.H., 2010, Glacial sea sur- R.C., et al., eds., Encyclopedia of geology: Volume 5: Ingle, J.C., Jr., 1973, Neogene history of the Gulf of Cali- face temperature of the East Sea (Japan Sea) inferred Oxford, Elsevier Academic Press, p. 503–520. fornia: Geological Society of America Abstracts with from planktonic foraminiferal assemblage: Geosci- Gradstein, F.M., Ogg, J.G., and Smith, A.G., eds., 2004, A Programs, v. 5, no. 1, p. 62. ences Journal, v. 14, p. 127–134, doi:10 .1007 /s12303 geologic time scale 2004: Cambridge, Cambridge Uni- Ingle, J.C., Jr., 1974, Paleobathymetric history of Neogene -010 -0013 -5 . versity Press, 589 p., doi: 10 .1017 /CBO9780511536045 . marine sediments, northern Gulf of California in Gas- Levander, A., Schmandt, B., Miller, M.S., Liu, K., Karl- Gross, E.L., Patchett, P.J., Dallegge, T.A., and Spencer, til, G., and Lillegraven, J., eds., Geology of peninsular strom, K.E., Crow, R.S., Lee, C.-T.A., and Humphreys, J.E., 2001, The Colorado River system and Neogene California: Los Angeles, Pacifi c Section, American E.D., 2011, Continuing Colorado plateau uplift by sedimentary formations along its course: apparent Association of Petroleum Geologists Guidebook, delamination-style convective lithospheric down- Sr isotopic connections: Journal of Geology, v. 109, p. 121–138. welling: Nature, v. 472, p. 461–465, doi:10 .1038 p. 449–461, doi: 10 .1086 /320793 . Ingle, J.C., Jr., 1980, Cenozoic paleobathymetry and depo- /nature10001 . Hamilton, W.B., 1960, Pliocene (?) sediments of salt water sitional history of selected sequences within the south- Linnaeus, C., 1758, Systema Naturae: per regna tria naturae, origin near Blythe, southeastern California: U.S. Geo- ern California continental borderland in Ingle, J.C., Jr., secundum classes, ordines, genera, species, cum char- logical Survey Professional Paper 400-B, p. B276– et al., eds., Studies in marine micropaleontology and acteribus, differentiis, synonymis, locis: Volume 1 B277. paleoecology: A memorial volume to Orville L. Bandy: (tenth edition): Leipzig, G. Engelman, 824 p.

Geosphere, October 2014 867

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/5/842/3333907/842.pdf by guest on 26 September 2021 McDougall and Miranda

Lucchitta, I., 1972, Early history of the Colorado River in Montagu, G., 1803, Testacea Britannica, or natural history of Resig, J.M., 1974, Recent foraminifera from a landlocked the Basin and Range province: Geological Society of British shells, marine, land and fresh-water, including Hawaiian lake: Journal of Foraminiferal Research, v. 4, America Bulletin, v. 83, p. 1933–1948, doi: 10 .1130 the most minute: Romsey, England, J.S. Hollis, 606 p. p. 69–76, doi: 10 .2113 /gsjfr .4 .2 .69 . /0016 -7606 (1972)83[1933: EHOTCR]2.0 .CO;2. Muller, D., Sdrolias, M., Gaina, C., Steinberger, B., and Resig, J.M., 1989, Stratigraphic distribution of late Neogene Lucchitta, I., 1979, Late Cenozoic uplift of the southwestern Heine, C., 2008, Long-term sea level fl uctuations species of the planktonic foraminifer Streptochilus in Colorado Plateau and adjacent lower Colorado River driven by ocean basin dynamics: Science, v. 319, the Indo-Pacifi c: Micropaleontology, v. 35, p. 49–62, region: Tectonophysics, v. 61, p. 63–95, doi:10 .1016 p. 1357–1362, doi: 10 .1126 /science.1151540 . doi: 10 .2307 /1485536 . /0040 -1951 (79)90292-0 . Olmsted, F.H., 1972, Geology of the Laguna Dam 1/2–min- Resig, J.M., 1993, Cenozoic stratigraphy and paleocean- Malmon, D.V., Howard, K.A., and Hillhouse, J.W., 2011, ute quadrangle, Arizona and California: U.S. Geo- ography of biserial planktonic foraminifera, Ontong Observations of the Bouse Formation in Chemehuevi logical Survey Geological Quadrangle Map GQ-1014, Java Plateau, in Berger, W.H., et al., Proceedings of and Parker Valleys, California and Arizona in Beard, scale 1:24,000. the Ocean Drilling Program, Scientifi c results, Volume L.S., et al., eds., CRevolution 2—Origin and evolu- Olmsted, F.H., Loeltz, O.J., and Irelan, B., 1973, Geohydrol- 130: College Station, Texas, Ocean Drilling Program, tion of the Colorado River system, workshop abstracts: ogy of the Yuma area, Arizona and California: U.S. Geo- p. 231–244, doi: 10 .2973 /odp .proc .sr .130 .014 .1993 . U.S. Geological Survey Open-File Report 2011–1210, logical Survey Professional Paper 486-H, p. H1–H227. Resig, J.M., and Kroopnick, P.M., 1983, Isotopic and dis- p. 204–205. Olsen, S., 1944, Danish Charopbyta: Chronological, ecologi- tributional evidence of a planktonic habit for the fora- Matoba, Y., and Oda, M., 1982, Late Pliocene to Holocene cal and biological investigations: Det Kongelige Danske miniferal genus Streptochilus Bronnimann and Resig, planktonic foraminifers of the Guaymas Basin, Gulf Videnskabernes Selskabs Skrifter, v. 3, p. 1–240. 1971: Marine Micropaleontology, v. 8, p. 235–248, of California, Sites 477 through 481, in Curray, J.R., Otvos, E.G., Jr., 1978, Calcareous benthic foraminiferal doi: 10 .1016 /0377 -8398 (83)90026 -9 . et al., eds., Initial reports of the Deep Sea Drilling Proj- fauna in a very low salinity setting, Lake Pontchartrain, Reynolds, S.J., Florence, F.P., Welty, J.W., Roddy, M.S., ect, Volume 64: Washington, D.C., U. S. Government Louisiana: Journal of Foraminiferal Research, v. 8, Currier, D.A., Anderson, A.V., and Keith, S.B., 1986, Printing Offi ce, p. 1003–1026, doi: 10 .2973 /dsdp .proc p. 262–269, doi: 10 .2113 /gsjfr .8 .3 .262 . Compilation of radiometric age determinations in Ari- .64 .144 .1982 . Patterson, R.T., 1987, Arcellaceans and foraminifera form zona: Arizona Geological Survey Bulletin 197, 258 p. Matti, J.C., and Morton, D.M., 1993, Paleogeographic evo- Pleistocene Lake Tecopa, California: Journal of Reynolds, R.E., Miller, D.M., and Bright, J., 2008, Possible lution of the San Andreas fault in southern California: Foraminiferal Research, v. 17, p. 333–343, doi:10 .2113 Bouse Formation in the Bristol Lake basin, California, A reconstruction based on a new cross-fault correla- /gsjfr .17 .4 .333 . in Reynolds, R.E., ed., Trough to trough: The Colorado tion, in Powell, R.E., et al., eds., The San Andreas fault Patterson, R.T., McKillop, W.B., Kroker, S., Nielsen, E., and River and the Salton Sea: Proceedings of the 2008 system: Displacement, palinspastic reconstruction, and Reinhardt, E.G., 1997, Evidence for rapid avian-medi- Desert Symposium: Fullerton, California State Univer- geologic evolution: Geological Society of America ated foraminiferal colonization of Lake Winnipegosis, sity, and Desert Studies Consortium and LSA Associ- Memoir 178, p. 107–159, doi: 10 .1130 /MEM178 -p107 . Manitoba, during the Holocene Hypsithermal: Journal ates, Inc., p. 62–67. Matti, J.C., Morton, D.M., and Cox, B.F., 1985, Distribution of Paleolimnology, v. 18, p. 131–143, doi:10 .1023 /A: Roskowski, J.A., Patchett, P.J., Spencer, J.E., Pearthree, and geologic relations of fault systems in the vicinity of 1007927622654 . P.A., Dettman, D.L., Faulds, J.E., and Reynolds, A.C., the central Transverse Ranges: U.S. Geological Survey Pawlowski, J., Bolivar, I., Farhni, J., and Zaninettii, L., 1995, 2010, A Late Miocene–Early Pliocene chain of lakes Open-File Report 85–365, 27 p. DNA analysis of “Ammonia beccarii ” morphotypes: fed by the Colorado River: Evidence from Sr, C, and Mattick, R.E., Olmsted, F.H., and Zohdy, A.A.R., 1973, One or more species?: Marine Micropaleontology, O isotopes of the Bouse Formation and related units Geophysical studies in the Yuma area, Arizona and v. 26, p. 171–178, doi: 10 .1016 /0377 -8398 (95)00022 -4 . between Grand Canyon and the Gulf of Califor- California: U.S. Geological Survey Professional Paper Pearthree, P., and House, K., 2014, Paleogeomorphology nia: Geological Society of America Bulletin, v. 122, 726-D, p. D1–D36. and evolution of the early Colorado River inferred from p. 1625–1636, doi: 10 .1130 /B30186 .1 . McDougall, K., 2008a, Late Neogene marine incursions and relationships in Mohave and Cottonwood Valleys, Ari- Ruiz, F., Rodriquez-Ramirez, A., Caceres, L.M., Vidal, J.R., the ancestral Gulf of California, in Reheis, M.C., et al., zona, California and Nevada: Geosphere, v. 10, doi:10 Carretero, M.I., Clemente, L., Munoz, J.M., Yanez, eds., Late Cenozoic drainage history of the southwest- .1130 /GES00988 .1 (in press) . C., and Abad, M., 2004, Late Holocene evolution of ern Great Basin and lower Colorado River region: Geo- Peterson, M.S., 1975, Geology of the Coachella Fanglomer- the southwestern Donana National Park (Guadalquivir logic and biotic perspectives: Geological Society of ate, in Crowell, J.C., ed., San Andreas fault in southern Estuary, SW Spain): A multivariate approach: Palaeo- America Special Paper 439, p. 355–373, doi:10 .1130 California: California Division of Mines and Geology geography, Palaeoclimatology, Palaeoecology, v. 204, /2008 .2439 (16) . Special Report 118, p. 119–126. p. 47–64, doi: 10 .1016 /S0031-0182 (03)00721 -1 . McDougall, K., 2008b, California Cenozoic biostratig- Phleger, F.B., 1964, Patterns of living benthonic foraminif- Rymer, M.J., Sarna-Wojcicki, A.M., Powell, C.L., II, and raphy—Paleogene, in Hosford Scheirer, A., ed., Petro- era, Gulf of California, in Van Andel, T.H., and Shor, Barron, J.A., 1994, Stratigraphic evidence for late Mio- leum systems and geologic assessment of oil and gas in G.G., Jr., eds., Marine geology of the Gulf of Califor- cene opening of the Salton Trough in southern Cali- the San Joaquin Basin Province, California: U.S. Geo- nia: A symposium American Association of Petroleum fornia: Geological Society of America Abstracts with logical Survey Professional Paper 1713, 30 p. Geologists Memoir 3, p. 377–394. Programs, v. 26, no. 2, p. 87. McDougall, K., 2011, Update on microfossil studies in the Poirrier, M.A., and Partridge, M.R., 1979, The barnacle, Rymer, M.J., Powell, C.L., II, Sarna-Wojcicki, A.M., and northern Gulf of California, Salton Trough, and lower Balanus subalbidus, as a salinity bioindicator in the Barron, J.A., 1995, Late Miocene stratigraphic and Colorado River, in Beard, L.S., et al., eds., CRevolu- Oligohaline estuarine zone: Estuaries, v. 2, p. 204–206, paleogeographic setting of Garnet Hill in the north- tion 2—Origin and evolution of the Colorado River doi: 10 .2307 /1351738 . western Salton Trough, southern California: American system, workshop abstracts: U.S. Geological Survey Poulson, S.R., and John, B.E., 2003, Stable isotope and trace Association of Petroleum Geologists Bulletin, v. 79, Open-File Report 2011–1210, p. 218–221. element geochemistry of the basal Bouse Formation p. 596. McDougall, K., Poore, R.Z., and Matti, J., 1999, Age and carbonate, southwestern United States: Implications d’Orbigny, A., 1839, Forminiferes, in Sagra, R. de la, ed., paleoenvironments of the Imperial Formation near San for the Pliocene uplift history of the Colorado Pla- Histoire physique, politique et naturelle de l’ile de Gorgonio Pass, southern California: Journal of Forami- teau: Geological Society of America Bulletin, v. 115, Cuba: Paris, France, A. Bertrand, 224 p., doi: 10 .5962 niferal Research, v. 29, p. 4–25. p. 434–444, doi: 10 .1130 /0016 -7606 (2003)115 <0434: /bhl .title .51128. McHugh, C.M.G., Gurung, D., Giosan, L., Ryan, W.B.F., SIATEG>2 .0 .CO;2 . Sarna-Wojcicki, A.M., Deino, A.L., Fleck, R.J., McLaughlin, Mart, Y., Sanca, U., Burckle, L., and Cagatay, M.N., Powell, C.L., II, 1995, Paleontology and signifi cance of the R.J., Wagner, D., Wan, E., Wahl, D., Hillhouse, J.W., 2008, The last reconnection of the Marmara Sea (Tur- Imperial Formation at Garnet Hill, Riverside County, and Perkins, M., 2011, Age, composition, and areal key) to the world ocean: A paleoceanographic and California: U.S. Geological Survey Open-File Report distribution of the Pliocene Lawlor Tuff, and three paleoclimatic perspective: Marine Geology, v. 255, 95–0489, 10 p. younger Pliocene tuffs, California and Nevada: Geo- p. 64–82, doi: 10 .1016 /j .margeo .2008 .07 .005 . Proctor, V.W., 1961, Batophora from central New Mexico: sphere, v. 7, p. 599–628, doi: 10 .1130 /GES00609 .1 . Metzger, D.G., 1968, The Bouse Formation (Pliocene) of Phycologia, v. 1, p. 160–163, doi: 10 .2216 /i0031 -8884 Schmalhausen, O.L., 1950, A new foraminiferal species the Parker-Blythe-Cibola area, Arizona and California, -1 -4 -160 .1 . from Lake Balpash-Sor (Kasakhstan): Doklady Aka- in Geological Survey Research 1968: U.S. Geological Quinn, H.A., and Cronin, T.M., 1984, Micropaleontology demii Nauk SSSR, v. 75, no. 6, p. 869–872. Survey Professional Paper 600-D, p. D126–D136. and depositional environments of the Imperial and Schnitker, D., 1974, Ecotypic variation in Ammonia bec- Metzger, D.G., and Loeltz, O.J., 1973, Geohydrology of the Palm Spring Formations, Imperial Valley, California, carii (Linnk): Journal of Foraminiferal Research, v. 4, Needles area, Arizona, California, and Nevada: U.S. in Rigsby, C.A., ed., The Imperial Basin—Tectonics, p. 217–223, doi: 10 .2113 /gsjfr .4 .4 .217 . Geological Survey Professional Paper 486-J, 54 p. sedimentation and thermal aspects: Los Angeles, Cali- Shafi qullah, M., Damon, P.E., Lynch, D.J., Reynolds, S.J., Metzger, D.G., Loeltz, O.J., and Irelan, B., 1973, Geo- fornia, Pacifi c Section, Society of Economic Paleon- Rehrig, W.A., and Raymond, R.H., 1980, K-Ar geohydrology of the Parker-Blythe-Cibola area, Arizona tologists Mineralogists, p. 71–85. chronology and geologic history of southwestern Ari- and California: U.S. Geological Survey Professional Rauzi, S.L., 1999, Index of samples of wells drilled for oil zona and adjacent areas: Arizona Geological Society Paper 486-G, 130 p. and gas in Arizona: Arizona Geological Survey Open- Digest, v. 12, p. 201–259. Miller, K.G., Wright, J.D., Browning, J.V., Kulpecz, A., File Report OFR 99–14, 18 p. Smart, C.W., and Thomas, E., 2006, The enigma of early Kominz, M., Naish, T.R., Cramer, B.S., Rosenthal, Y., Riedel, F., Kossler, A., Tarasov, P., and Wunnermann, B., Miocene biserial planktic foraminifera: Geology, v. 34, Peltier, W.R., and Sosdian, S., 2012, High tide of the 2011, A study on Holocene foraminifera from the Aral p. 1041–1044, doi: 10 .1130 /G23038A .1 . warm Pliocene: Implications of global sea level for Sea and west Siberian lakes and its implication for Smith, P.B., 1960, Fossil foraminifera from the southeast- Antarctic deglaciation: Geology, v. 40, p. 407–410, migration pathways: Quaternary International, v. 229, ern California deserts: U.S. Geological Survey Profes- doi: 10 .1130 /G32869 .1 . p. 105–111, doi: 10 .1016 /j .quaint .2010 .03 .009 . sional Paper 400-B, p. B278–B279.

868 Geosphere, October 2014

Downloaded from http://pubs.geoscienceworld.org/gsa/geosphere/article-pdf/10/5/842/3333907/842.pdf by guest on 26 September 2021 Marine incursion, Colorado River corridor

Smith, P.B., 1964, Ecology of benthonic species: U.S. Geo- Spencer, J.E., Patchett, P.J., Pearthree, P.A., House, P.K., morphologic variability: Journal of Foraminiferal logical Survey Professional Paper 429-B, 55 p. Sarna-Wojcicki, A.M., Wan, E., Roskowski, J.A., and Research, v. 20, p. 128–156, doi: 10 .2113 /gsjfr .20 .2 Smith, P.B., 1969, Pliocene (?) foraminifera of the lower Faulds, J.E., 2013, Review and analysis of the age and .128 . Colorado River area, California and Arizona, in origin of the Pliocene Bouse Formation, lower Colo- Wennrich, V., Meng, S., and Schmiedl, G., 2007, Foramini- Abstracts of Papers Submitted for the Meeting in rado River Valley, southwestern USA: Geosphere, v. 9, fers from Holocene sediments of two inland brackish Boze man, Montana May 7–12 1968, in Abstracts for p. 444–459, doi: 10 .1130 /GES00896 .1 . lakes in central Germany: Journal of Foraminiferal 1968: Geological Society of America Special Paper Stouff, V., Geslin, E., Debenay, J.P., and Lesourd, M., 1999, Research, v. 37, p. 318–326, doi:10 .2113 /gsjfr .37 .4 121, p. 560–561, doi: 10 .1130 /SPE121 -p585 . Origin of morphological abnormalities in Ammonia .318 . Smith, P.B., 1970, New evidence for Pliocene marine (Foraminifera); studies in laboratory and natural envi- Winker, C.D., 1987, Neogene stratigraphy of the Fish embayment along the lower Colorado River area, ronments: Journal of Foraminiferal Research, v. 29, Creek–Vallecito section, southern California: Implica- California and Arizona: Geological Society of America p. 152–170. tions for early history of the northern Gulf of California Bulletin, v. 81, p. 1411–1420, doi:10 .1130 /0016 -7606 Stump, T.E., 1972, Stratigraphy and paleontology of the and Colorado Delta [Ph.D. thesis]: Tucson, University (1970)81 [1411: NEFAPM]2 .0 .CO;2. Imperial Formation in the western Colorado desert of Arizona, 494 p. Spencer, J.E., and Patchett, J.P., 1997, Sr isotope evidence [M.S. thesis]: San Diego, California State University, Winker, C.D., and Kidwell, S.M., 1986, Paleocurrent evi- for a lacustrine origin for the upper Miocene to Plio- 132 p. dence for lateral displacement of the Pliocene Colo- cene Bouse Formation, lower Colorado River trough, Taylor, D.W., 1983, Late Tertiary mollusks from the Lower rado River delta by the San Andreas fault system, and implications for timing of Colorado Plateau Colorado River valley: University of Michigan Con- southeastern California: Geology, v. 14, p. 788–791, uplift: Geological Society of America Bulletin, v. 109, tributions from the Museum of Paleontology, v. 26, doi: 10 .1130 /0091 -7613 (1986)14 <788: PEFLDO>2 .0 p. 767–778, doi: 10 .1130 /0016 -7606 (1997)109 <0767: p. 289–298. .CO;2 . SIEFAL>2 .3 .CO;2 . Terquem, O., 1876, Essai sur le classement des animaux qui Winker, C.D., and Kidwell, S.M., 1996, Stratigraphy of Spencer, J.E., and Pearthree, P.A., 2001, Headward erosion vivent sur la plage et dans les environs de Dun kerque; a marine rift basin: Neogene of the western Salton versus closed-basin spillover as alternative causes of deuxieme fascicule: Dunkerque, France, Societe Trough, California, in Abbott, P.L., and Cooper, J.D., Neogene capture of the ancestral Colorado River by the Dunkerquoise, Memoire, v. 20, 159 p. eds., Field conference guidebook and volume for the Gulf of California, in Young, R.A., and Spamer, E.E., Thornton, S.E., Pilkey, O.H., and Lynts, G.W., 1978, A American Association of Petroleum Geologists Annual eds., The Colorado River: Origin and evolution: Grand lagoonal crustose coralline algal micropridge: Bahiret Convention (San Diego, California, May 1996): Canyon, Arizona, Grand Canyon Association Mono- el Bibane, Tunisia: Journal of Sedimentary Research, Bakersfi eld, California, Pacifi c Section, American graph 12, p. 215–219. v. 48, p. 743–749. Association of Petroleum Geologists, p. 295–336. Spencer, J.E., Pearthree, P.A., Patchett, J.P., and House, P.K., Todd, T.N., 1976, Pliocene occurrence of the recent atherinid Winterer, J.I., 1975, Biostratigraphy of Bouse Formation: A 2005, Evidence for a lacustrine origin for the lower fi sh Colpichthys regis in Arizona: Journal of Paleon- Pliocene Gulf of California deposit in California, Ari- Pliocene Bouse Formation, lower Colorado River Val- tology, v. 50, p. 462–466. zona, and Nevada [M.S. thesis]: Long Beach, Califor- ley, in Reheis, M.C., ed., Geologic and biotic perspec- Turak, J., 2000, Revaluation of the Miocene/Pliocene depo- nia State University, 132 p. tives on late Cenozoic drainage history of the south- sitional history of the Bouse Formation, Colorado Wood, R.D., 1952, An analysis of ecological factors in the western Great Basin and lower Colorado River region: River trough, southern Basin and Range (CA, NV, and occurrence of C. baraceae of the Woods Hole region, U.S. Geological Survey Open-File Report 2005–1404, AZ) [M.S. thesis]: Laramie, University of Wyoming, Massachusetts: Ecology, v. 33, p. 104–109. p. 14. 96 p. Zalat, A.A., 1995, Calcareous nannoplankton and diatoms Spencer, J.E., Pearthree, P.A., and House, P.K., 2008, Valle-Levinson, A., 2010, Defi nition and classifi cation of from the Eocene/Pliocene sediments, Fayoum Depres- An evaluation of the evolution of the latest Miocene estuaries, in Valle-Levinson, A., ed., Contemporary sion Egypt: Journal of African Earth Sciences, v. 20, to earliest Pliocene Bouse lake system in the lower issues in estuarine physics: Cambridge, Cambridge p. 227–244, doi: 10 .1016 /0899 -5362 (95)00056 -Y . Colorado River valley, southwestern USA, in Reheis, University Press, p. 1–11. Zullo, V.A., and Buising, A.V., 1989, An unusual species M.C., et al., eds., Late Cenozoic drainage history of the Walton, W.R., 1955, Ecology of living benthonic foraminif- of the Balanus amphitrite Darwin complex (Cirripe- southwestern Great Basin and lower Colorado River era, Todos Santos Bay, Baja California: Journal of dia, balanidae) from the late Cenozoic Colorado River region: Geologic and biotic perspectives: Geological Paleontology, v. 29, p. 952–1018. delta in western Arizona and southeastern California: Society of America Special Paper 439, p. 375–390, doi: Walton, W.R., and Sloan, B.J., 1990, The genus Ammo- Biological Society of Washington Proceedings, v. 102, 10 .1130 /2008 .2439 (17) . nia Brunnich, 1772: Its geographic distribution and p. 924–932.

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