Clumped isotopes

Clumped isotopes are heavy

The equilibrium constants for these reactions are temperature-dependent, with a tendency for heavy isotopes to "clump" with each other (increasing the proportions of multiply substituted isotopologues) as temperature decreases.[9] Reaction 1 will be driven to the right with decreasing temperature, to the left with increasing temperature. Therefore, the equilibrium constant for this reaction can be used as an paleotemperature indicator, as long as the temperature dependence of this reaction and the relative abundances of the carbonate ion isotopologues are known.

Differences from the conventional δ¹⁸O analysis

In conventional δ¹⁸O analysis, both the δ¹⁸O values in carbonates and water are needed to estimate paleoclimate. However, for many times and places, the δ¹⁸O in water can only be inferred, and also the ¹⁶O/¹⁸O ratio between carbonate and water may vary with the change in temperature.^[10][11] Therefore, the accuracy of the thermometer may be compromised.

Whereas for the carbonate clumped-isotope thermometer, the equilibrium is independent of the isotope compositions of waters from which carbonates grew. Therefore, the only information needed is the abundance of bonds between rare, heavy isotopes within the carbonate mineral.

Methods

1. Extract CO₂ from carbonates by reaction with anhydrous phosphoric acid.^[12][13] (there is no direct way to measure the abundance of CO₃²⁻s in with high enough precision). The phosphoric acid temperature is often held between 25° and 90 °C^[14] and can be as high as 110 °C.^[15][16]
2. Purify the CO₂ that has been extracted. This step removes contaminant gases like hydrocarbons and halocarbons which can be removed by gas chromatography.^[17]
3. Mass spectrometric analyses of purified CO₂, to obtain δ¹³C, δ¹⁸O, and Δ47 (abundance of mass-47 CO₂) values. (Precision needs to be as high as ≈10⁻⁵, for the isotope signals of interest are often less than ≈10^−3.)

Applications

Paleoenvironment

Clumped isotopes analyses have traditionally been used in lieu of conventional δ¹⁸O analyses when the δ¹⁸O of seawater or source water is poorly constrained. While conventional δ¹⁸O analysis solves for temperature as a function of both carbonate and water δ¹⁸O, clumped isotope analyses can provide temperature estimates that are independent of the source water δ¹⁸O. Δ47-derived temperature can then be used in conjunction with carbonate δ¹⁸O to reconstruct δ¹⁸O of the source water, thus providing information on the water with which the carbonate was equilibrated.^[18]

Clumped isotope analyses thus allow for estimates of two key environmental variables: temperature and water δ¹⁸O. These variables are especially useful for reconstructing past climates, as they can provide information on a wide range of environmental properties. For example, temperature variability can imply changes in solar irradiance, greenhouse gas concentration, or albedo, while changes in water δ¹⁸O can be used to estimate changes in ice volume, sea level, or rainfall intensity and location.^[14]

Studies have used temperatures derived from clumped isotopes for varied and numerous paleoclimate applications — to constrain δ¹⁸O of past seawater,^[18] pinpoint the timing of icehouse-hothouse transitions,^[19] track changes in ice volume through an ice age,^[20] and to reconstruct temperature changes in ancient lake basins.^[21][22]

Paleoaltimetry

Clumped isotope analyses have recently been used to constrain the paleoaltitude or uplift history of a region.^[23][24][25] Air temperature decreases systematically with altitude throughout the troposphere (see lapse rate). Due to the close coupling between lake water temperature and air temperature, there is a similar decrease in lake water temperature as altitude increases.^[26][24] Thus, variation in water temperature implied by Δ47 could indicate changes in lake altitude, driven by tectonic uplift or subsidence. Two recent studies derive the timing of the uplift of the Andes Mountains and the Altiplano Plateau, citing sharp decreases in Δ47-derived temperatures as evidence of rapid tectonic uplift.^[23][27]

Atmospheric science

Measurements of Δ47 can be used to constrain natural and synthetic sources of atmospheric CO₂, (e.g. respiration and combustion), as each of these processes are associated with different average Δ47 temperatures of formation.^[28][29]

Paleobiology

Measurements of Δ₄₇ can be used to better understand the physiology of extinct organisms, and to place constraints on the early development of

A key premise of most clumped isotope analyses is that samples have retained their primary isotopic signatures. However, isotopic resetting or alteration, resulting from elevated temperature, can provide a different type of information about past climates. For example, when carbonate is isotopically reset by high temperatures, measurements of Δ47 can provide information about the duration and extent of metamorphic alteration. In one such study, Δ47 from late Neoproterozoic Doushantou cap carbonate is used to assess the temperature evolution of the lower crust in southern China.^[32]

Cosmochemistry

Primitive meteorites have been studied using measurements of Δ47. These analyses also assume that the primary isotopic signature of the sample has been lost. In this case, measurements of Δ47 instead provide information on the high-temperature event that isotopically reset the sample. Existing Δ47 analyses on primitive meteorites have been used to infer the duration and temperature of aqueous alteration events, as well as to estimate the isotopic composition of the alteration fluid.^[33][34]

Ore deposits

An emerging body of work highlights the application potential for clumped isotopes to reconstruct temperature and fluid properties in hydrothermal ore deposits. In mineral exploration, delineation of the heat footprint around an ore body provides critical insight into the processes that drive transport and deposition of metals. During proof of concept studies, clumped isotopes were used to provide accurate temperature reconstructions in epithermal, sediment hosted, and Mississippi Valley Type (MVT) deposits.^[35][36] These case studies are supported by measurement of carbonates in active geothermal settings.^[35][37][38]

Limitations

The temperature dependent relationship is subtle (−0.0005%/°C).^{[citation needed]}

¹³C¹⁸O¹⁶O₂²⁻ is a rare isotopologue (≈60 ppm [3]).

Therefore, to obtain adequate precision, this approach requires long analyses (≈2–3 hours) and very large and uncontaminated samples.

Clumped isotope analyses assume that measured Δ47 is composed of ¹³C¹⁸O¹⁶O₂²⁻, the most common isotopologue of mass 47. Corrections to account for less common isotopologues of mass 47 (e.g. ¹²C¹⁸O¹⁷O ¹⁶O²⁻) are not completely standardized between labs.

See also

• δ¹⁸O
• δ¹⁵N
• δ¹³C
• Paleothermometer
• Isotopic signature
• Isotope analysis
• Isotope geochemistry
• Isotopic labeling

References