QUATERNARY RESEARCH 13, 172 -186 (1980) Holocene Desert Soil Formation under Sodium Salt Influence in a Playa-Margin Environment FREDERICK F. PETERSON Plant, Soil. Water Science Dil'isiotl. Unil'ersity (~r Ne\'ada. Renu. Reno. Nevada 89557 Received March 20. 1979 A visually prominent desert soil with a horizon of clay accumulation (Typic Natrargid) has formed under an arid climate in Panamint Valley, California, in sandy, very calcareous, saline fan alluvium in less than about 3500 yr, and probably less than 2000 yr. Such soils can be used as stratigraphic markers, but could be confused with other desert soils with clay-accumulation horizons (Haplargids) which occur much more commonly on desert alluvial fans, are mostly late Pleistocene or older, and do not form in parent materials that are still calcareous. This Natrargid formed in a playa-margin environment, where clay for translocation and sodium salts that engender rapid clay movement probably were provided by dust fall. INTRODUCTION Soil horizons can serve as stratigraphic markers for geomorphic and archeological studies of Quaternary deposits. Some soils also can be age indicators, but for either use the pedogenic status of the soil horizons, their kind and degree of alteration, and the conditions of formation should be explicitly identified to prevent misinterpretations. Layers merely identified as "weakly" or "strongly developed soil horizons" may be such for reason of soil structure, consistence, the relative color, clay, calcium carbonate, or opal content, or combinations of these properties. Too frequently, no evidence is given for pedogenic alteration, as compared with geologic origin, and the rather different times and conditions of formation for different pedogenic alterations are not considered. Clay, carbonate, or opal accumulation-to form argillic, calcic or petrocalcic horizons, or duripans-are the most prominent evidences of soil formation in arid regions, and we now have considerable understanding of rates and conditions for their pedogenic accumulation. This paper describes relatively rapid, pedogenic clay accumulation in the natric horizon of a Natrargid formed in highly calcareous alluvium, apparently under conditions of 172 0033-5894/80/020172-15$02.00/0 Copyright © 1980 by the University of Washington. All rights of reproduct.ion in any form reserved. marked soil salinity and aridity. 1 Natrargids 2 are a subclass of Aridisols, or pedogenic desert soils, having a B horizon of both iHuvial clay and exchangeable sodium accumulation called a natric horizon (USDA, 1975, p, 28, 163). The more common Haplargids-which have an analogous ilIuvial clay B horizon, or argillic horizon, but lack significant exchangeable sodium accumulation in it-most commonly occur on late Pleistocene or older surfaces and do not seem to form in even moderately calcareous parent material until the carbonate has been leached. These two similar desert soils can be confused. Both can serve as stratigraphic markers, but their implied ages and formation conditions are quite different. In arid, southern New Mexico, a few Haplargids with minimal argillic horizons have formed in as little as 1100-2100 yr in high-gravel (i.e., >50% by volume), lowcarbonate (i.e., <2% CaC0 3 equivalent) J This work was part of an unpublished. cooperative archaeological study directed by E. L. Davis. Great Basin Foundation, San Diego. Calif. It was done while the author was a member of the Soils and Plant Nutrition Department, University of California, Riverside. 2 In the literature prior to about 1970, Natrargids were included among soils called "Solonetz" or "Solodized-Solonetz" soils. 173 HOLOCENE PLAYA-MARGIN SOILS parent materials. The youngest Haplargids buffer (Grossman and Millet, 1961). The in low-gravel, low-carbonate parent mate- percentage water-soluble salts and CaC03 rials are some 2200-4600 yr old. These equivalents were calculated from weight parent materials either contained some clay losses after dialysis. Soluble salt concenfor translocation, or the soils received clay tration in a saturated paste extract was as dust fall. Soils with argillic horizons do measured by conductivity, and the sodium not occur in high-carbonate (i.e., > 15% adsorption ratio (SAR) was determined from CaC0 3 equivalent) parent materials of soluble-cation concentrations (Richards, Holocene age (Gile, 1975, pp. 356-357). 1954). Cation exchange capacity was meaHowever, most desert soils with argillic sured by the method of Okazaki et al. (1962). horizons formed in either high- or low- Organic matter was determined by wet oxicarbonate parent materials in this area are dation (Richards, 1954). Soil pedon descripoflate Pleistocene age, or older, and appar- tions and identifications follow soil survey ently formed primarily under more effective terminology (USDA, 1975). leaching conditions of pluvial intervals STUDY SITE DESCRIPTION cooler and moister than the Holocene (Gile The Natrargids described here occur on and Hawley, 1968, p. 715). In arid western an alluvial-fan skirt at Lake Hill, a small Nevada, where argillic horizons formed in dolomite hill in northern Panamint Valley, arkosic sands, chemical weathering and California (Fig. 1). This valley is a long clay movement have been too slow to form structural basin bounded on the east by the argillic horizons in less than 12,000 yr, or Panamint Range and on the west by the since the late Pleistocene (Nettleton et al., Argus Range. Playas separated by a low 1975). In such areas, desert soils with argilalluvial divide now occur at the vaHey's lic horizons and low gravel contents can be thought of as late Pleistocene or older relicts. Natric horizons can form relatively much more rapidly in low-gravel, high-carbonate, clay-containing parent materials under the dispersive influence of sodium. Many occur on sediments no older than late Pleistocene, or in playas, or on the margins of present or c_ wI' Pleistocene lakes in situations suggesting -,-T ,.L Holocene age (USDA, 1975, pp. 19, 28, / 163). Alexander and Nettleton (1977) reported Natrargid formation in less than en 'P' 6600 yr in loamy, calcareous 0- 3% CaC0 3 ~ equivalent), saline (conductivity of satura~ -\ tion extract = 4-30 mmhos/cm), floodplain -1J sediments in arid western Nevada. This I' V V (" paper describes an even more rapid Natrar"'N " v gid formation in a yet more calcareous, '" '" I v-t7"' more saline material. -<.l -- (;) ,/ ('0 METHODS Particle-size analyses were made by pipet method for fine earth from which (a) soluble salts were removed by protracted dialysis against water, and (b) carbonates were removed by protracted dialysis against pH 5 ~ 0 0 0_5 '1-" km FIG. I. Location of the Lake Hill, Panamint Valley, California site, the bulldozer-cut exposures, and the major landforms. 174 FREDERICK F. PETERSON north and south ends, but roughly 100km-Iong and 280-m-deep Pleistocene lakes fed by local drainage and spillover from the Pleistocene Searles - China - Owens Lakes system periodically filled the Panamint basin until it, in turn, spilled over into Death Valley as late as Tahoe time, and perhaps as late as early Tioga time. During latest Tioga time, a lake about 60 m deep filled the southern playa and a separate, very shaHow lake (about 6 m deep) filled the northern playa (Blackwelder, 1954: R. S. U. Smith, 1975, 1978). Lake Hill stands between the eastern shore of the I3-km-Iong northern playa and the toeslope ofthe 2- to 4-km-wide al1uvial-fan piedmont of the Panamint Range. The playa (472-m elevation) is 0.6-1.3 km wide west of Lake Hill, and extends 9 km to the south: both are directions from which storm winds carry eolian sediments. The Argus Range alluvial-fan piedmont, to the west, is some 6 km wide. The Panamint Valley floor is arid, hot in summer, and cold enough for transitory snowfall in winter. Mean annual precipitation is only 10 em, but much comes from regional winter storms that have been seen to moisten effectively a shallow soil layer. Mean-maximum July temperature is 41°C, and mean-minimum January temperature is OQC (Elford, 1970). Except for sparse shrubs, e.g., creosote bush (Larrea tridentata), the study site is barren. The site proper comprises (1) the 145-mhigh, 3-km-Iong hill, (2) its surrounding 45to 140-m-wide, very gently sloping, anuvial-fan skirt grading to the playa, or to the Panamint-Range-fan piedmont, and (3) the playa. Lake Hill is a barren, rocky, sloping to steep-sided fault block of highly shattered and partially recemented, dense, grey dolomite. It has only a very shallow, rocky soil mantle. The playa is actively filling with verypale-brown (lOYR 7/3, dry; 10YR 5/4, moist), sticky, plastic, gravel-free, loamy sediments from the Panamint and Argus Ranges. The surficial playa sediment contains about 2% water-soluble salts. 20% calcium and magnesium carbonates, M1 sand (mostly fine and very fine sand), 7S7r silt, and 19o/r clay near the site. Roughly equal proportions of carbonate occur in the sand-, silt-, and clay-size fractions. Weathering and erosion of the Lake Hill dolomite mass itself must contribute only miniscule sediment to the playa, and its alluvial-fan skirt has been graded to a playa base level largely controlled by erosional events on the great fan piedmonts and mountain fronts. The Lake Hill fan-skirt sediments contain much dolomite sand and fine gravel from the hill's bedrock, but several relations suggest the finer material in the fan-skirt soil was blown from the playa and deposited directly on the fan skirt, or deposited on the hill and then washed back onto the fan skirt. First, eolian sand is now collecting as thin, discontinuous mantles at the base of the steep hillslopes and washing back onto the fan skirt through rills and distributary channels (Fig. 2). Second, the surficial playa sediment and fine earth component of the fan and hill soils have similar compositions and brownish colors when compared with the gray dolomite. The playa sediment and soils all have clay fractions in which montmorillonite is dominant, mica and kaolinite contents are moderate, and both calcite and dolomite are present. Their fine earth fractions are 20-40% carbonates, whereas the dolomite is about 95% carbonates. Third, the A and B horizons of the very shallow soil on gently sloping ridge crests just above the fan skirt apparently formed in eolian material. Since this soil is approximately contemporaneous with those of the hill slopes and fan skirt, or only slightly older, it is evidence that eolian material probably was deposited on the hill, from which it was available to be washed back onto the fan skirt. The ridge-crest soil has largely gravel-free A and B horizons with only 20- 26% carbonates in the fine earth. The underlying Cca horizon is considerably thinner than the combined A and B horizons, is extremely gravelly and stony, and HOLOCENE PLAYA-MARGIN SOILS 175 FIG. 2. A low scarp between the modern Rainbow fan surface. in the foreground, and remnants of the late-Holocene Lake Hill fan surface. The spade is stuck in an outcrop of the natric horizon formed on the Lake Hill surface. A thin mantle of eolian sand lies at the base of the rocky slopes of the dolomite hill. The Panamint Range is in the far background . . ' grades to shattered dolomite bedrock which contains only 5% acid-insoluble residue. If the approximately 75% noncarbonate material of the A and B horizons is residue from weathering of the dolomite under an arid climate, much larger volumes of pedogenic carbonates would be expected to have accumulated in the Cca horizon than occur. Both the low gravel content of the A and B horizons, and the small volume of pedogenic carbonate, suggest eolian deposition. ALLUVIAL-FAN SKIRT The datable Natrargid occurs on the 15to 33-m-wide, alluvial-fan skirt on the west side of Lake Hill. Maximum fan slopes are about 7% at the top, but most are from 4 to less than 2%. The fan abuts the steep hill slopes abruptly and its gravel-paved al- luvium has a distinct terminus on the playa. The fan skirt comprises two differently aged surfaces. The older, relatively stable Lake Hill fan surface is marked by the prominent, though thin, grey Av horizon 3 and reddish-brown B2t horizon of a Natrargid, and is being shallowly dissected in many places (Fig. 2). The resultant, younger, inset, Rainbow fan surface heads at the hill sideslopes, is cut from a few to about 30 cm deep into the older surface, and grades onto the playa beyond remnants of the older surface. The younger surface has a thin, grey Av horizon, but either only :l The" Av" horizon notation is an informal one denoting vesicular porosity; it is not found in official soil survey pedon descriptions. There these massive. crusting. vesicularly porous. surficial horizons are noted as Al horizons. 176 FREDERICK 1'. PETERSON an incipient, slightly reddened B2 horizon, or no B2 horizon. It has common distributary rills across it and is an active surface of sediment transport. Eroding outcrops of the reddish-brown nat ric horizon at the scarped margins of the older Lake Hill surface remnants suggest the younger surface is being expanded laterally. In some places, fresh distributary rills still cross Lake Hill surface remnants, but most hillslope drainage bypasses the older surface and flows across the younger. Both fan surfaces have a sparse desert pavement of 1- to 3-cm dolomite pebbles and coarse sand; pebbles are somewhat more closely spaced on the older surface. Artifacts (i.e., exotic obsidian chips) are found on both surfaces and in the fan alluvium under at least the older surface. The Rainbow surface is a modern surface contemporaneous with the playa, to which it grades, and with active portions of the Panamint and Argus fan piedmonts which also grade to and feed sediment to the playa. The Lake Hill surface toeslope merges topographically with the Rainbow surface. The distinctive, reddish-brown natri c horizon of the Lake Hill surface ends where the two surfaces apparently merge: no exposures were seen where Rainbow sediments overlie and bury the Lake Hill surface soil horizons. ALLUVIAL-FAN SKIRT AND PLAYA SEDIMENT STRATIGRAPHY Sediments underlying the alluvial-fan skirt and playa margin were exposed in three bulldozer cuts, originally numbered 1. 2, and 6. Stratigraphy was established in cut 6, and confirmed in the other two cuts (Figs. 1, 3, and 4). The sediments separate into two units of major significance: an upper unit of merging alluvial-fan skirt (AF) and playa (AP) sediments (AFAP, where imbricated), and a lower unit of basal fan gravel (BF) and basal lacustrine (BL) sediment. Pleistocene Basal Sediments From about station 12 (meters, horizontal distance) on out past station 29, in cut 6 (Fig. 3a), the major unconformity between the units is underlain and marked by a distinctively grayish, very friable loam or gravelly loam Alb horizon (i.e., a buried horizon of humus accumulation), which has 4% oxidizable humus, as compared with the humus-free overlying sediment. The Alb horizon is underlain by a carbonate-rich, light-gray (N 7/, dry; N 5/, moist) silt loam horizon beyond station 19. This peculiar horizon is shot through with l-mmdiameter, vertical, yellowish-brown-claycoated root channels. Because it has the prominent clay skins characteristic of many argillic horizons, it is noted as a B2tb horizon in Fig. 3. Between stations 12 and 19, the Alb horizon is underlain by a white, friable, highly carbonate-impregnated, gravelly loam Ccab horizon, which looks like marl and is so different in site and character from the Cca horizons of the hill soils that it is informally called the "marly" horizon (M) here. This horizon also is shot through with vertical 2- to 3-mm-diameter root channels, but these are surrounded by a hard, white, carbonate encrustation. Below these adjacent B2tb and "marly" horizons is a 5- to 8-cm-thick, black, peaty-feeling Ob horizon (i.e., buried organic soil horizon) which contains some 7% oxidizable humus. and considering its consistence. probably a much larger amount of nonoxidizable, carbonized, peaty organic material. A sample taken at station 16 was dated at 10,020 ± 120 HC yr B.P. (UCLA-989). Between stations 14 and 15, the Ob horizon divides into numerous, thin, gray layers that merge into the "marly" horizon. and suggest alternating deposition of humus-rich sediment and marl. Several thin. dark-gray layers of apparent humus accumulation occur between the Alb and Ob horizons, indicating that the sediment which buried the Ob horizon accumulated slowly enough to allow periodic humus accumulation. In cut 2 (Fig. 4), carbonized reeds taken from the upper part of a correlative Alb horizon dated at 10,520 ± 140 HC yr B.P. (UCLA-990). A correlative Alb also occurs in cut I (Fig. 3b). The Alb and eA) - Cut 6. north wall upper playa margin, 35m .. --- Lake Hill ton surface ---- .. ,Av.:...~ ..."- "'':_'''"'_'''''':.'''.-'''''"'''''''''"'''''''''''''''fl"",·,""""m:''(;-;A:-:F~);-::"~",~""~",:::;"";;;;~,;;;;",,,,,,"""";;;"";r,;",m",,;;;l;.,,,;m,,,ii 'lIi iul,i i'Iijjljlliilllliililiiilliiilllil1d,iiilliillliiiIITiniiil!Iiii!!'iiiTu 82t 1IIIIIIillll" ' _'-"; ------- -- --------------------3" 83 .~ .....~-:i!e'" Gm~...... 30 .. -3 Q; E ...... ~'.r.'.I.!! U.'\ll tIt r~)·'-..J\>l(BF) "~I: 2'5 ~~~-c.~.. ··)"i.,,-M....,...~r-- (AP) ~k"1'l"M~«.~/~#~Alb :/Ii ? .... _ _:.t.: • !it----- 82 tb II) ::r:: or o("j m z -4 \ dated Ob horizon 10.020 ± 120 14C yr B.P (UCLA 9S9) 2'0 '0 1'5 5 6 m ." r ~ ~ hillslope-0 -.. If'~I"v.; ~Av .......... .'~J~. "'"'82f 2- 4- . 6- o .... ··Ceo dolomite bedrock > -< )- (B) Cut I, south wall Hill fan surface --- - - ....... -mergence lone - -- --~"--Roinbow i:)- fan surface--- .... ~ Z playa margin. 9m - playa surface level- . 10 ;.. . 20 . meters 30 '"o r::: '" (AP) ... ~p~fj);pp}1'~#~ 40 50 FIG. 3. Stratigraphic diagrams for bulldozer cuts 6 and 1 on the Lake Hill alluvial-fan skirt. Members of the basal Pleistocene unit are: (BL) basal lacustrine sediments, and (BF) basal fan gravel. Members of the overlying Holocene unit are: (AP) playa sediment, (AF) alluvial-fan-skirt alluvium, (AFG) very gravelly f;m alluvium, and (AFAP) imbricated fan and playa sediment. Soil horizon notation is explained in the text; soil lithological discontinuity notations are not used. Vertical exaggeration is 1.5 x . .... -.I -.I 178 FREDERICK F. PETERSON Cut 2. east wall ~ __ Rainbow fan surface----: ·Lake Hili fan surface -2 IO,520! 140 14C yr BP subhorizons , , 15 10 4 (UCLA 990) 5 0 meters FIG. 4. Stratigraphic diagram for bulldozer cut 2 in the Lake Hill alluvial-fan skirt. See Fig. 3 for key to symbols. Vertical exaggeration is 1.5 x . Ob horizons, or zone of humus accumulation, date the basal lacustrine sediments as late Pleistocene. Since "marly"-horizon sediments overlap the basal fan gravel (BF), it is as old or older. Although only some of the dolomite pebbles and cobbles in the basal fan gravel are rounded, and the gravel is not stratified, it does occur in a position that suggests it could be a poorly worked beach deposit. Its large pebbles and cobbles (8-13 cm diameter), compared with the fine gravel of the later alluvial-fan skirt, might also reflect strong erosional stripping of Lake Hill in late Pleistocene time. Carbonate coatings are common on the bottoms of pebbles and suggest that the basal fan gravel contains a relict Ccab horizon, but there is no evidence of an overlying, relict B horizon. The Ob horizon (Fig. 3a) is so peaty it would be expected to have formed in a continuously wet regime, i.e., a shallow lake margin or marsh. Pollen from this horizon " ... showed sedges and cattails (Typha tatifolia or hybrids of T. lat(folia) were locally abundant" (Mehringer, 1967, p. 187). The overlying Alb horizon probably formed in a moist. but occasionally dry regime, for it has a lower humus content and nonpeaty consistence. The underlying, discontinuous, or pod-like "marly" horizon exposed in cuts I and 6 may have formed at the edge of a marshy area by biological car- bonate precipitation, or. as suggested by the carbonate root-casts. by plant transpiration and resultant carbonate precipitation from bicarbonate-charged water. The root casts suggest that the marl deposition and humus accumulation in the Alb horizon occurred contemporaneously. The neutral grey matrix color of the 82tb horizon underlying the Alb and Ob horizons also suggests a strongly reducing environment of a marsh or shallow lake bottom. However, the yellowish and reddish-brown color of the c1ayskins that line the open, vertical root channels and some cracks between blocky structural units do not indicate reducing conditions. In cut 6, these clay-lined root channels and cracks extend from below the Ob horizon up through it to the base of the Alb horizon, and indicate that clay deposition occurred after the Ob horizon was buried, and that the Alb horizon formed under less-wet, perhaps periodically dry conditions. The clayskins probably were formed by pedogenic clay iIluviation because they originate at the base of the Alb horizon, but they might have been deposited by infiltration of muddy water during the first stages of burial of the Alb horizon by Holocene playa sediment. Holocene Sediments The Lake Hill alluvial-fan skirt is formed of finely stratified coarse sand and fine gravelly sandy loam (AFG) in its upper parts, but rapidly grades to finely stratified medium sand, loamy fine sand, and fine sandy loam with common, thin, discontinuous strata of coarse sand and fine dolomite gravel toward its toeslope (AF). At about station 16 (Fig. 3a) the fan alluvium abruptly thins and is underlain by stratified, gravel-free. coarse sand-free, pale-brown, and light-grey playa deposits of well-sorted medium sand, loamy fine sand, very fine sandy loam, and coarse silt textures (AP). All fan and playa sediments are calcareous and saline. Several 2- to 50-em-thick and meter-wide lenses of gypsum and salt-cemented fine HOLOCENE PLAYA-MARGIN SOILS gravel (Gm) occur both in otherwise uncemented gravel (AFG) and as isolated, cemented gravel lenses in the middle reaches of the fan at 60- to 9O-cm depth. Similar cemented lenses were found at about the same contour in pits along the fan skirt, including the soil-sampling site (Table 1). They are not regularly related to the overlying natrie horizon, and are interpreted as erratic concentrations of salts in these very saline sediments, rather than as a pedogenic horizon. Playa and Fan Sediment Ages The playa sediments overlying the Alb and Ob horizons are less than about 10,000 yr old. Because the alluvium forming the 179 Lake Hill and Rainbow fan surfaces overlaps or grades to the playa sediment, it is no older, and probably younger, than the upper playa deposits (Fig. 3). A closer dating for the Holocene playa deposits may be inferred by correlation with stratigraphically very similar deposits in the China Lake and Searles Lake basins, just southwest of the Panamint basin. Those adjacent basins were occupied by shallow Holocene lakes related to a pluvial event beginning about 4000-6000 yr ago, and ending about 2000-3000 yr ago (Smith and Davis, 1978, pp. 167, 172). At Searles Lake, the uppermost lacustrine deposit is identified by Smith (1968) as the "Overburden Mud" unit, or alternatively as unit "D" (G. I. TABLE 1 PEDON DESCRIPTION FOR THE NATRARGID ON THE LAKE Hill Sl:RFACE COMPONEl"T OF THE ALLUVIAL FAl" SKIRT" Horizon/ Depth (cm) Description Pavement 1-0 Dolomite pebbles. \- 3 cm diameter. solution pitted and unpitted. not varnished, cover 5·-10% of surface; quartz and dolomite very coarse sand covering 15~90% of surface. Av 0-0.6 Light-gray (lOYR 6/1) sandy loam, grayish-brown (lOYR 5/2) moist; massive, cracked into 6 to to-cm polygons; hard, friable. slightly sticky, nonplastic; violently effervescent; abrupt smooth boundary to: B2t 0.6-20 Light-reddish-brown (5YR 6/4) sandy clay loam grading to loam with depth, reddish-brown (5YR 4/4) moist; weak medium to coarse prismatic grading to massive with depth; slightly hard, very friable, sticky. plastic; violently effervescent; a few fine gypsum crystals: clear wavy boundary to: B3 20-41 Banded, or lamellar light-reddish-brown (5YR 5/6) fine sandy loam and lightgray (lOYR 7/1) fine sand, reddish-brown and gray (5YR 4/4 and IOYR 6/1) moist; massive; slightly hard to loose. very friable to loose, nonsticky. nonplastic: about ¥.J of horizon consists of the 1- to 2-cm-wide, light-reddishbrown bands of clay-coated sand which are more widely spaced with depth; violently effervescent; abrupt smooth boundary to: Cl 41-51 Light-gray (10YR 61l} fine sandy loam to silt loam. grayish-brown (lOYR 512) moist; massive; hard, firm, non sticky , nonplastic: violently effervescent; slakes in water; many fine gypsum crystals: similar 10 "Gm"-cemented lenses occurring in cui 6; abrupt smooth boundary to: C2m 51-53 Light-gray (I0YR 6/1) sandy loam, dark gray (lOYR 4/1) moist; massive; strongly cemented by salts; violently effervescent: like the "Gm"-cemented lenses occurring in cut 6, " Distributary rills were braided across the soil surface at this sampling site some 15 m downslope from the upper fan margin and 8 m north of cut 6 (Fig. 3A), /i Lithological discontinuities (USDA, 1975, p. 462) involving contrasting textures or mineralogies inherited from parent material strata are not noted since they are potentially numerous in this stratified alluvium, and since all horizons but the C horizon are postulated to have been sand or loamy sand textured initially. The relatively silty C horizon probably was formed from sediments quite contrasting to the overlying sandy fan alluvium. 180 FREDERICK F. PETERSON Smith, 1978); it appears to correlate with the playa deposit (AP) at Lake Hill, Panamint Valley. Deposition of Searles Lake unit "D" was followed by a period of soil formation (Smith, 1968, p. 304); the Natrargid on the Lake Hill alluvial-fan skirt would be correlative with that soil. The deposition of the Searles Lake unit "D" was preceded by a period of complete lake recession and soil formation (" soil CD," Smith and Davis, 1978, p. 168; G. I. Smith, 1978, p. 4); the Alb- B2tb soil that formed in basal lacustrine sediment (BL) at the Lake Hill site is correlative. The period of "CD" soil formation at Searles Lake was preceded by deposition of the "Parting Mud," or unit "C," which is older than about 10,000 yr (G. I. Smith, 1968, 1978); the basal lacustrine sediment below the Ob horizon is older than 10,000 yr and correlative with unit "C." The correlation of the Lake Hill site playa sediment (AP) with the Searles Lake unit "D" is considered reasonable by G. I. Smith (personal communication, 1978), but he emphasized that the only firm date for unit "D" is from a piece of wood found near the middle of this unit which had an age of 3520 ± 120 HC yr B.P. (Stuiver, 1964). Since the Lake Hill fan-skirt alluvium (AF), and in particular that forming the .. Lake Hill surface," is no older, and probably younger, than the playa sediments (AP), then the fan surface can be considered at least younger than 3500 yr and probably younger than 2000 yr. The soil formed on the Lake Hill fan surface is, therefore, probably younger than 2000 yr. THE LATE HOLOCENE SOIL The soil 4 on the Lake Hill fan surface will be shown to be pedogenic, hence indicative of geomorphic stability and, thus, stratigraphically significant. It is a fine-loamy, , In the most general sense, soil is merely earthy material which contains living material and is potentially capable of supporting plants (USDA, 1975, p. I): thus soil can be fresh geologic alluvium essentially unaltered by genetic soil-forming processes, or a pedogenic body. mixed, thermic Typic Natrargid;' (USDA, 1975, pp. 163 164). Pedogenic soils may be defined as those containing one or more altered layers, or horizons, which parallel a present land surface (or buried or exhumed surface) and which are somewhere discordant with the geologic structure or fabric of their parent materials. Altered means an addition to, or loss from, or mechanical rearrangement of what reasonably can be assumed to have been the parent material (i.e., "geologic" material as contrasted with resultant "pedogenic" soil). The alteration, such as humus, or clay, or carbonate accumulation or loss, or soil structure formation, characterizes the layer and ditIerentiates it from underlying or overlying layers. Parallelism to a land surface is evidence that the alteration is somehow related to processes dependent on infiltration of meteoric water from the land surface to generally uniform depths, but in variable amounts and frequencies for different depth zones with different etIects. Thus, ilIuvial clay must accumulate below a source or transmittal horizon-the eluvial A horizon-and pedogenic CaCO;! will accumulate at yet greater depth at the limit of common moisture penetration in arid climates. Discordance with parent material structure or fabric demonstrates that the alteration postdates emplacement or formation of the parent material. Discordance can be megascopic, as where an entire argillic horizon passes with angular discordance through weathered, dipping, geologic strata which have been truncated by an erosion surface, or as where a petrocalcic horizon passes from well-sorted alluvium into contiguous, hillslope, colluvial deposits. Or, the discordance may be a nearly microscopic relation to fabric, as where illuvial clay in an argillic horizon bridges and cements alluvial sand grains and pebbles in a fashion never seen in the freshly deposited :, The properties of most. but not all the pedons (or sampling volumes) satisfy the taxonomic criteria: this is the usual situation when soils are mapped and identified according to the U.S. Soil Taxonomy (USDA. 1975). HOLOCENE PLAYA-MARGIN SOILS material, or as in a prismatic cambic horizon where the horizontal, fine stratifications of a sediment have been disrupted and mixed, and vertical cracks now appear. The Av horizon and B2t horizon, or natric horizon, of the Natrargid are both pedogenic, but only the latter is taxonomically diagnostic and geomorphically or stratigraphically significant. The soil does not have a significant pedogenic carbonate horizon; the salt - gypsum impregnated or cemented Cl and C2 horizons encountered in the sample pedon (Table 1; cf., "Gm" lenses, Fig. 3a) are discontinuous and, as stated above, are not considered pedogenic horizons. The Av and B2t horizons are 15 and 30 cm thick, respectively, on the uppermost fan segment (Fig. 3a, stations 0-2), where the alluvium from which the pedogenic horizons formed was coarsest (a loamy medium to coarse sand), but they rapidly thin downslope and are only about 5 and 18 cm thick at stations 9 to 16, where the alluvium was medium sand, and are a mere 1 and 7 cm thick at station 23, where the alluvium was a fine sand or fine sandy loam. Beyond station 29, where the Lake Hill fan surface terminates, and the younger Rainbow fan surface replaces it, there is a 1em-thick Av horizon, but only the slightest reddening suggests formation of an incipient cambic B. The thinning solum may be explained by the increasing waterholding capacity of the progressively finer-textured fan sediments downslope, hence shallower precipitation infiltration. Additionally, sheetflood irrigation from the hills lopes should be lesser and more widely or erratically distributed downslope, and effective wetting could have been less. Where sampled (Table 1), the Av horizon is only 0.5-1 cm thick; rills cross the surface here and may have slightly eroded the soil. However, except for thickness, the horizon is characteristic for the soil. The thin Av horizon is light-colored, has very low humus content, and is massive except for a coarsely polygonal pattern of des- 181 iccation cracks. When dry it forms a slightly hard or hard crust, with prominent 1- to 2-mm-diameter vesicular pores. Massiveness, polygonal cracking, crusting, and vesicular porosity are features diagnostic of surficial loamy soil materials that slake readily and have been repeatedly saturated and dried. Size and number of vesicular pores increase with recurrent saturation-desiccation cycles if the material is not crushed by wheel or animal traffic (cf., Miller, 1971). Such Av horizons form in materials as coarse as loamy sand and as fine as clay loam, but are most common in sandy loams or silt loams with low clay and humus contents. They can form in only a few months. An A v horizon is the first horizon to form in sand-within a few hundred years, or less-where dust falls on the sand and is infiltrated; since dust fall seems ubiquitous in deserts, this is a significant soil-forming process (Gile, 1975; Peterson, 1977; Yaalon and Ganor, 1973). The 1em-thick Av horizon in the modern, sandy, Rainbow surface soil is evidence of rapid formation. The A v horizon has only a sparse desert pavement of unvarnished pebbles, but a thin, very coarse sand mulch covers 15-90% of the surface and obscures the polygonal crack pattern. Desert pavements are prominent on arid-region soils that contain gravel and occur where dust or loess fall has been slow, or minimal. However, the Av horizon which regularly occurs under the desert pavements, or without a pavement, is an ubiquitous characteristic of desert soils. The clay increase from A to B horizon (Table 2 and illuvial clay deposits described later) qualify the B as an argillic horizon and its very high SAR value and prismatic structure qualify it as a natric horizon (Table 2). Much of the clay-size fraction is carbonate, and both carbonate and silicate clay contents increase from A to B horizon; cation exchange capacities confirm the acid-insoluble clay distribution (Table 3). This soil is extremely saline and sodic. 182 FREDERICK F. PETERSON TABLE 2 PARr/elf-SIZE DISTRIBUTION OF [HE WHOLE SOIL A~[) IHE SOLUBLE. S.-\U-FREE A"ID C\RBON.UE-FREF FINE EARTH FOR THE LAKE HILL SURFACE NATRARGlD Fine earth (<;;. of soluble-salt-free fine earth) Horizon Av B2t B2t B3 B3 CI Depth (em) 0-0.6 0.6-13 13-20 20-30 30-41 41-51 Whole soil v.eo.s. 1-2 mm (%) >5 mm 5-2 mm <2 mm 5 4 6 4 3 3 1 3 <1 3 <1 10 89 86 93 96 94 99 co.s. 1-0.5 mm m.s. 0.5-0.25 mm f. ,. 0.25~O.1 mm S" C" S C S C S C 16 11 6 2 2 10 5 3 6 9 4 5 5 3 4 3 9 6 8 8 16 6 5 4 6 9 16 14 II 19 34 6 14 10 12 1 0 11 8 11 18 4 Fine earth (% of soluble-salt-free fine earth) v.f.s. Horizon Av B2t B2t B3 B3 Cl Depth (em) 0-0.6 0.6-13 13-20 20-30 30-41 41-51 0.1-0.05 mm Total Sand 2-0.05 mm Silt 0.05-0.002 mm Clay <0.002 mm ._------ S C S C S C S C 19 16 12 25 28 26 18 14 II 18 18 16 66 56 41 64 92 35 53 40 30 38 49 22 20 16 25 19 2 53 17 14 12 17 8 26 14 28 34 17 6 12 10 20 CaCO" equiv. 23 13 4 8 20 26 35 32 39 44 " The S columns are for the soluble-salt-free, <2-mm fine earth after dialysis against water. " The C columns for the soluble-salt- and carbonate-free fine earth after dialysis against pH 5 buffer. Sodium is the dominant water-soluble cation, followed by Ca, Mg, and even a significant K accumulation. The soluble anions are dominantly chloride with some carbonate-bicarbonate accumulation in lower horizons. Soluble sulfate approximates a saturated gypsum solution (27 me/liter); undoubtedly larger amounts of gypsum are present than dissolved (Table 3). The highly calcareous nature of all horizons and particle-size classes, except possibly the silt fraction in the lower B3 horizon, is indicated by the decreasing percentage of each fraction after protracted dialysis against pH 5 buffer (Table 2). The increased silt content of the acid-treated lower B3 horizon material may have been due to accumulation of silty acid-insoluble residue from decomposed dolomite sand. The particularly high proportions of carbonate silt and clay in the lower B2t and C 1 horizons suggest some carbonate precipitation there. Total fine-earth CaCO;j equivalents range from 20 to 30% in the solum, levels which seem to preclude clay iIluviation in soils lacking dispersive exchangeable sodium. Contiguous Soils Bulldozer cut number I extended up onto a bedrock spur of Lake Hill (Fig. 3b) and showed that the A v and B2t horizons of the fan-skirt Natrargid continue onto the hillslopes in what are inferred to be eolian fines trapped between bedrock outcrops. A pedon sampled on top of a gently sloping ridge crest has a I-em-thick Av horizon, a HOLOCENE PLAYA-MARGIN SOILS 183 7-cm-thick, strong medium columnar, loam, natric B2t horizon, an 8-cm-thick, massive, loam B3 horizon, and a to-cmthick, white, very gravelly loam IICca horizon over shattered, carbonate-impregnated bedrock. This soil has 22-26% CaCO:l equivalent for its gravel-free solum, and is saline in its B2t, B3, and IICca horizons. It is afine-Ioamy, mixed, thermic, Lithic Natrargid. The soil of the younger Rainbow fan surface is a coarse-loamy, mixed, thermic Typic Torriorthent. The soil of the adjacent playa is afine-loamy, mixed. thermic Typic Torriorthent. SOIL GENESIS O.."...".<nt-'¢ o\~~oo~""': 8N '£:: o :I: The pedogenic and illuvial nature of the B2t horizon, and the pedogenic and eluvial nature of the Av horizon are demonstrated by several lines of evidence. Both horizons approximately parallel the land surface; variations in thickness and depth are related to probable fan-alluvium texture, as previously described, and can be explained by effective leaching depth. The clay accumulated in the B2t uniformly coats and prominently reddens skeletal sand grains; hence it has altered the horizon. Where the alluvium was coarsesand textured, the thin clay coatings can be seen bridging between sand grains in a fashion discordant with the original fabric of the alluvium. Clay deposition in the B3 horizon is in 1- to iO-mm-thick bands, or lamellae, within which the sand grains are coated and bridged by reddish-brown clay; sand grains between lamellae are grayish and clean. The lamellae both follow and cut across fine alluvial stratification with angular discordance. Clay bridging and lamellae are most prominent at the upper, coarsest textured end of the fan skirt. Illuvial and pedogenic clay lamellae are common in sandy parent materials 10 humid regions (i.e., udic soil-moistureregime areas) (Dijkerman et al .. 1967). The author has seen them frequently in xeric soils and several times in aridic soils. In these latter two cases, at least, lamellae are the first morphological forms of illuvial clay 184 FREDERICK F. PETERSON deposition in clean sands, in some sandy illuviation of the clay fraction. The ratios of loams, and some low-clay, silt-loam parent both total and acid-insoluble silt to clay materials. In relatively very young sedi- percentages in the A v and B2t horizons ments the lamellae occur throughout the shows that not only does clay content in· B-horizon depth zone: with continued clay crease, but it increases relative to silt con· illuviation those in the upper part of this tent from the A v to B2t horizon. If dust had zone are masked by overall illuvial clay infiltrated without some preferential clay coating, but clay illuviation seems to cease eluviation, the ratio of silt to clay would in the B3 position and the lamellae there are have remained constant. preserved. When clay accumulation in the Attributing the source of clay and silt to B2 position is great enough for soil shrink· dust infiltration also helps explain the rela· ing and swelling to create soil structure, tively great thickness and clay content of lamellae are completely obscured. the natric horizon when compared with relOn the middle and lower fan skirt, where atively thin A v horizon, which traditionally clay accumulation has altered the texture of is considered the source of illuvial clay. (At parent material from sandy loam to clay four sites along cut 6, other than the sample loam, shrinking and swelling has created site, the B2t horizon is 1.7,3.6,7.0, and 4.0 weak to moderate, coarse prismatic or col- times as thick as the Av horizon: the B2t umnar structure in the B2t horizon. In some horizon has somewhat more than twice the places there even has been infiltration of percentage clay content as the A v horizon). grayish A v·horizon material into the cracks Where dust fall and infiltration are active, between the columnar peds. This soil an A horizon may act more nearly as a structure is additional evidence of discor· transport zone for eolian clay, and some dance, and of the pedogenic nature of the silt, than as a clay source. There is common B2t horizon. Not only silicate clay, but also evidence of dust fall and infiltration in carbonate clay, appears to have accumu· Nevada, New Mexico, and other desert lated in the B2t horizon, relative to the Av areas (Peterson, 1977: Gile, 1975: Yaalon horizon, since the proportion of carbonate and Ganor, 1973). in the clay fraction is similar throughout the Effective dispersion of the calcareous solum. As significantly, hoth the Av and clays by sodium salts is suggested by very B2t horizons are markedly finer textured turbid pools that collect in microdepres· than the B3 horizon, or the sand or loamy sions at the periphery of the fan skirt after sand C horizon of fan alluvium occurring heavy storms. Clay remains in suspension below the B3 horizon over much of the for several days until the water evaporates. soil's extent (cf., Fig. 3a). Since the fan al· The fan Natrargid is so saline (e.g .. the satluvium probably was originally a sand or uration extract of the Av horizon is 0.9 N; loamy sand throughout (as seems reason· Table 3) that one might suspect salt floccu· able for at least the upper fan) and since the lation would prevent clay dispersion and materials are young and still highly calcare· eluviation. However, the soil samples were ous, and have been subject to only the lim- collected from dry soil; surface salt ited leaching of an arid environment, it does efflorescences in spots on the dry soil indinot seem reasonable that the silt and clay cate capillary salt movement to, and concontents of the solum are products of centration in, the surface soil as it dries. chemical weathering. They may be attrib- During a storm, the Av horizon should be uted to infiltration of eolian dust, either de· leached to some lower salt concentration posited directly or washed from the hill and clay should disperse. As a qualitative across the fan. The dispersive influence of test of clay flocculation by salts, Avsodium should have aided infiltration of horizon material was equilibrated by four both silt and clay, and is hypothesized to centrifuge washings with 0.1, 0.2, 0.3. 0.4. account for the preferential eluviation and 0.5, and 0.6 N NaCI. After the final cen- HOLOCENE PLAYA-MARGIN SOILS trifuging, which should have sedimented all flocculated clay, all supernatants were still somewhat turbid. The surface layer of apparently clayey sediment occupied at least twice the volume, when equilibrated with 0.6 N NaCI, as its weight percentage would suggest. The clayey sediment showed increased volume, or water imbibition against centrifugal force, with decreasing salt concentration; in 0.1 N NaCl some four times greater volume occurred than expected if the clay were tightly flocculated. This marked swelling suggests that under heavy storms or sheetflood irrigation, at least clayey aggregate spalling should occur in this salty soil, thus releasing clay for eluviation. Soluble-salt distribution suggests some downward translocation and accumulation in the lower B2t horizon, and perhaps a yet earlier accumulation in the C horizon. Because the surficial playa sediments are saline, the salt in the Natrargid solum probably accumulated along with the postulated eolian silt and clay. Part of the salt, and particularly the halite and gypsumcemented "Gm" lenses in the C horizon, may have accumulated from saline groundwater as the playa sediments were being deposited. In either case, Na for clay dispersion should have been present during soil formation. CONCLUSIONS The Typic N atrargid of the Lake Hill fan-skirt surface is pedogenic because clay accumulation altering the parent alluvium of its natric horizon is discordant with both stratification and fabric of the alluvium, and because the horizon parallels the land surface. Clay. and probably silt, illuviation has occurred in very calcareous and saline parent material under an arid climate. Apparently both carbonate and silicate clay have translocated under the dispersive influence of sodium salts. The soil has formed in less than about 10,000 yr as inferred by radiocarbon dating at the site, or in less than about 3500 yr by stratigraphic correlation to radiocarbon-dated sediment in the 185 adjacent Searles Lake basin, and probably in less than about 2000 yr by correlation with the period of deposition proposed for the analogous Searles Lake sediment. The dispersive sodium salts and clay for translocation probably were provided from the adjacent playa by dust falL The similar Haplargids, or non-sodiumaffected desert soils with a horizon of illuvial clay accumulation, most commonly are late Pleistocene age or older and do not form in still strongly calcareous parent materials. Natrargids, such as this one in Panamint Valley, could be confused with Haplargids only cursorily studied, and their age and conditions of formation misinterpreted. REFERENCES Alexander, E. B .. and Nettleton, W. D. (\977). Post-Mazama Natrargids in Dixie Valley, Nevada. Soil Science Sociery of America Journal 41, 1210-1212. Blackwelder. E. (1954). Pleistocene lakes and drainage in the Mojave region, southern California. In "Geology of Southern California, Part 5" (R. H. Jahns, Ed.), pp. 35-40. California Division of Mines, San Francisco. Dijkerman, J. C., Cline, M. G., and Olson. G. W. (1%7). Properties and genesis of textural subsoil lamellae. Soil Science 104, 7 -15. Elford. C. R. (1970). "Climates of the States: Climate of California." Climatography ofthe U.S. No. 60-4. U.S. Dept. Commerce, Environ. Sci. Servo Admin., Silver Springs. Md. Gile, L. H. (19751. Holocene soils and soil-geomorphic relations in an arid region of southern New Mexico. Quaternary Research 5, 321- 360. Gile. L. H., and Hawley, J. W. (\%8). Age and comparative development of desert soils at the Gardner Spring radio-carbon site. New Mexico. Soil Science Society of America Proceedings 32, 709-716. Grossman, R. B., and Millet, J. L. 096!). Carbonate removal from soils by a modification of the acetate buffer method. Soil Science Society 0/ America Proceedings 25, 325 - 326. Mehringer, P. J., Jr. (J%7). "Pollen Analysis of the Tule Springs Area. Nevada." Nevada State Museum Anthropological Papers No. 13. Part 5, pp. 129-200. Miller. D. E. (l971). Formation of vesicular structure in soil. Soil Science Society (~f America Proceedings 35, 635~637. Nettleton, W. D .. Witty, J. E .. Nelson, R. E .. and Hawley. J. W. (1975). Genesis of argillic horizons in 186 FREDERICK F. PETERSON soils of desert areas of the southwestern United States. Soil Sciem'l' Society "IAmerica Proceediflgs 39.919-926. Okazaki, R.. Smith. H. W .. and Moodie. C. D. (1962). Development of a cation exchange capacity proccdure with few inherent errors. Soil Science 93, 343-349. Peterson. F. F. (1977). "Dust Infiltration as a Soil Forming Process in Deserts." p. I Agronomy Abstracts, American Society of Agronomy. Los Angeles, Calif. Richards. L. A. (Ed.) (1954). "Diagnosis and Improvement of Saline and Alkali Soils." Agricultural Handbook 60. U.S. Dept. of Agriculture. Washington. D.C. Smith. G. I. (1968). Late Quaternary geologic and climatic history of Searles Lake. southeastern California. In .. Means of Correlation of Quaternary Successions" (R. B. Morrison and H. E. Wright. Jr .. Eds.). Vol. 8, pp. 293-310. [NQVA VII Congress. Smith. G.1. (1978). "Late Quaternary Geology of Searles Valley. California: A Field Guide." Informal Guidebook for Friends of the Pleistocene. Pacific Coast Section. n. Smith, G. I .. and Davis. E. [ (I'in). Late Wiscon;'llI-subrecent ~oib at China Lak\;!. "/ "The Ancient Californians. Rancholabrean Hunters of the Mojave Lake Country" IE. L. Davi.'. Ed.). pp. 167 --172. Natural History Museum of [.0' Angeles County. Science Series 29. Smith. R. S. U. (1975). "Late-Quaternary Pluvial and Tectonic History of Panamint Valley. Inyl) and San Bernardino Counties, California." Unpublished Ph.D. thesis. California Institute of Technology. Pasadena. Smith. R. S. U. (1978). "Pluvial History of Panamint Valley. California." Guidebook for Friends of the Pleistocene, Pacific Cell. Stuiver. M. (1964). Carbon isotopic distribution and correlated chronology of Searles Lake sediments. All/aiel/II .In/mllli of Sci<'llc{' 262, 377 - 39~. U.S. Department of Agriculture (19751. "Soil Taxonomy." Agricultural Handbook No. ~36. Washington, D.C. Yaalon. D. H .. and Ganor. E. (1973). The intluence of dust on soils during the Quaternary. Snil .\'ci(,II(,{, 116. 146-155.
© Copyright 2024 Paperzz