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135 I.E-Examining COSO OBSIDIAN HYDRATION RATES

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135 I.E-Examining COSO OBSIDIAN HYDRATION RATES NEW METHODS AND NEW QUESTIONS IN CALIFORNIA ARCHAEOLOGY 135 I.E- ExAMINING COSO OBSIDIAN HYDRATION RATES JEROME KING Obsidian hydration data on Coso obsian arttifacts from upland Pinyon Zone and lowland Volcanic Field localities in Inyo County show differences attributable to difference in effective temperature between the two areas. Data presented her shows that the magnitude of the difference becomes greater with increasing age. I address this problem by generating anew temperature correction factor and employing new hydration/radiocarbon pairings from recent research in Owens Valley to arrive at new calendric rate equations for both areas. The results underscore the importance ofeffective temperature as an overriding variable controlling the hydration process. ince its proposal ten years ago, Basgall's (1990) required by the Coso rate equation in order to bring hydration rate equation for Coso obsidian has each type's age estimates into the same approximate Sbeen successfully applied in a number of settings range. Further, the magnitude of the required throughout the southwestern Great Basin. This rate correction becomes greater with increasing age, equation was a great improvement over its many suggesting to Hildebrandt and Ruby that a predecessors, as it explicitly addressed temperature as fundamentally different approach to temperature the primary variable controlling local hydration rates. correction needed to be developed. Since that time some problems applying the rate have become apparent, particularly at the early end of the This paper attempts to address these problems by chronology, where it appears that the rate equation proposing yet another rate equation and temperature overestimates true age (Basgall 1993; Delacorte 1999). correction for Coso obsidian, employing new Also, problems have arisen in applying the rate in hydration/radiocarbon pairings from recent research in temperature settings markedly different from the Owens Valley, as well as some theoretical Owens Valley floor. considerations drawn from the literature on experimental obsidian hydration rate development. I For example, Hildebrandt and Ruby (1999) would like to turn first to the theoretical issues. compared samples of hydration measurements for various projectile point types from recent projects in two adjacent, but climatically very different, areas: the THEORETICAL CONCERNS Coso Volcanic Field, at about 4,000-ft elevation (Gilreath and Hildebrandt 1997), and the adjacent Researchers studying hydration rate development pinyon zone of the Coso Range, at elevations between have taken both experimental and empirical 7,000 and 8,000 ft (Hildebrandt and Ruby 1999). Both approaches, often producing results that are markedly data sets show reasonably well-distributed hydration at odds. While experimental rates have met with little values (Figure 1; Table 1), underscoring the general acceptance from many archaeologists attempting to utility of both obsidian hydration and projectile point reconcile real archaeological problems, they do have typologies as chronometric tools. However, large the advantage of incorporating a theoretical differences between the means for each type are understanding of the chemistry behind the process. apparent. All other things presumably being equal, This could profitably be considered when formulating these effects are due to the difference in effective empirical rates. Specifically, two issues are relevant to temperature between the two areas. While empirical rate derivation: the shape of the rate curve, temperature data are not available for the higher and approaches to temperature correction. pinyon zone, Hildebrandt and Ruby suggest that effective hydration temperature (EHT) ought to be on The first experimental hydration rate derivations the order of 7° C cooler there than in the lower zone. (Friedman and Long 1976; Friedman and Smith 1960) However, differences in EHT as great as 13° would be found that the process of obsidian hydration is similar Jerome King. Far Western Anthropological Research Group. Inc.• P. O. Box 413. Daris CA 9561 7 Proceedings of the Society for California Archaeology. Volume 14. 2004, pp 135-142 136 PROCUDI.VGS OF TIIf. SOCieTY fOR CALIFORNIA ARCHAEOLOGY, VOL. 14, 2000 18.0 -,----------------------, --+- Coso Range Figure 1, Table 1: Obsidian Hydration Values from 16.0 Pinyon Zone Coso Volcanic Field and Coso Range Pinyon Zone. ---- Coso Volcanic Field 14.0 note: all means recalculated excluding outliers via Chauvenet's criterion. 2- 12.0 C <L> E Pinyon Zone x n ~ 10.0 := (f) Desert Series 2.3 ± 0.8 49 CD <L> Rose Spring 3.0 ± 0.3 105 ~ 8.0­ o o@ Thin Elko 3.9 ± 1.2 39 u Little Lake/Pinto 6.6 ± 2.9 11 I' 6.0 Volcanic Field x n 4.0 Desert Series 3.0 ± 1.2 12 Pinto Series Rose Spring 5.2 ± 0.8 20 2.0 ­ Thin Elko 7.4±1.0 12 Desert Series 0.0 -L-__________________---' Little Lake/Pinto 12.8±3.4 12 to most diffusion processes in that it falls off with the argue that using the same rate exponent for all square root of time: obsidian sources is a parsimonious approach, because 2 it acknowledges that despite trace-element variability, t =x / k the basic chemical composition of all obsidians is where t equals time in years, x is the similar. In any case, many empirically-derived rate obsidian hydration measurement in equations, such as the present Coso rate, approach the microns, and k is a source- and square-root falloff model and could be recalculated to temperature-specific rate conStant. fit it with only marginal loss of fit to the data points. They found that this is common to all obsidians Another area where theory could better inform regardless of their (face-element chemis(fY. A number empirically-developed rates is that of temperature of experimental and empirical studies since then have correction. Basgall's (1990) Coso rate equation confirmed that the exponent in the equation ought to specifies that for each deg ree difference in EHT be two (Bouey 1995; Onken 1991; Tremaine 1987), between the base Lone Pine locality and the locality but researchers working with real archaeological being corrected , ~ 6 percent correction should be as emblages have generally ignored this constraint applied to the micron reading: when trying [0 fit hydration results with other chronological data, proposing instead exponents from x' = x(1 - 0.06[T'-TJ) as low as one (i.e., a purely linear formulation) to more than three. Like many empirically-derived rates, where x is the original micron reading, x' Basgall's Coso rate equation simply finds the best fit to is the corrected micron reading, T is the the data, resulting in an exponent of 2.32: base EHTat Lone Pine (16.85 °C), and T' is the EHT value for which the correction 2 32 t = 31.62x is applied. or, expressing the equation in the form given above, While this correction is easy to apply and works well within a certain temperature range, both ZJZ t = X /0.03162 experimental data and general theory indicate that the relationship between temperature and hydration rate I suggest instead that the experimental data are does not behave this way, and is instead logarithmic in strong enough that empirical rate formulations should nature (Friedman and Trembour 1984; Hull n.d.; Hull be bound by the simple square-root falloff rate. I also et af. 1995; Tremaine 1987). The rate of chemical NEW METHODS AND NEW QUESTIONS IN CAlIFORNIA ARCHAEOLOGY 137 reactions in relationship to temperature is expressed 10000 via the Arrhenius equation: - Logarithmic correction (E = 110000jlmol) 9000 k = Ae-E/RT - Arithmetic correction (6% I 0C) 8000 where kis the rate constant in the equations above, A is an empirically 7000 determined coefficient of reaction, e is a::- the base of natural logarithms (2.71828), e 6000 E is the reaction's activation energy in E joules per mole. R is the universal gas ·c 5000 *lfl constant (8.31 j/mol K), and T is the Q) reaction temperature in Kelvins. :;r 4000 To adjust a hydration rate equation for temperature 3000 effects, one calculates a new value not for the micron value, but for the rate constant k (Hatch et 01. 1990) : 2000­ k' = keE(lrr -I/T')/R 1000 where k is the rate constant at the base 0 EHT, k' is an EHT-corrected rate -15 -10 -5 0 5 10 15 EHT correction (OC) constant, T is the base EHT in Kelvins, and T' is the EHT to which the rate is Figure 2: Age estimates produced by the existing Coso rate being corrected, also in Kelvins. equation with a 6% per-degree correction vs. a logarithmic correction with an activation energy of 110,000 jlmol. While different from the arithmetic correction specified in Basgall's rate equation, this method of , correction still leaves one with the task of empirically available from sites further afield, this sample is determining the overall magnitude ofchange in rate in limited to southern Owens Valley, so that effective relation to temperature, which is expressed by the temperature can be treated as more or less constant. activation energy E. Five new data points are included here (Figure 3; To illustrate the differences between the two Table 2). For all five points, outlying hydration values methods, Figure 2 shows the age estimates produced have been excluded via Chauvenet's criterion and by the existing Coso rate equation with a 6 percent multiple radiocarbon dates averaged using Calib 4.2. per-degree correction vS ..a logarithmic correction with Only one of the points (from CA-INY-2750; see an activation energy of 110,000 j/mol, for a Delacorte 1999) is a discrete feature context similar to hypothetical specimen with a hydration measurement the original pairs from site CA-INY-30. The others are of 5.0 microns. This value for E is similar to the 13 based on single-component sites from which the entire percent-per-degree logarithmic correction that Onken hydration assemblage serves as a data point.
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