TRACING PALEOFLUID SOURCES USING CLUMPED ISOTOPE ...

TRACING PALEOFLUID SOURCES USING CLUMPED ISOTOPETHERMOMETRY OF DIAGENETIC CEMENTS ALONG THE MOAB

FAULT, UTAH

SARAH C. BERGMAN, KATHARINE W. HUNTINGTON†, and JULIET G. CRIDERDepartment of Earth and Space Sciences, University of Washington, Box 351310,

4000 15th Avenue NE, Seattle, Washington, 98195-1310

ABSTRACT. Interactions among fluids, deformation structures, and chemical changesin sediments impact deformation of the shallow crust, influencing the preservation andextraction of the economic resources it contains. These interactions have been studiedalong the Moab Fault, in the Paradox Basin, Utah, where diagenetic cements, joints,cataclastic deformation bands and slip surfaces developed during faulting are thoughtto control fault permeability. Previous fluid inclusion micro-thermometry and stableisotopic data from calcite cements collected along segments of the Moab Fault suggestcements precipitated from hot basin fluids that migrated up the fault and interactedwith a shallower meteoric groundwater source. In this study, we investigate theinteractions of these fluids with deformation structures using clumped isotope thermom-etry of calcite cements along the Moab Fault. Guided by prior high-resolution mappingof deformation structures and calcite cements, we measured the growth temperatureof calcite cements collected at varying distance from fault segments and fault intersec-tions. Cement temperatures from individual segments vary greatly; cements along arelatively simple fault segment indicate temperatures ranging from 67 to 128 °C,similar to previously published fluid inclusion homogenization temperatures from acement sample collected in the same locality, while a nearby fault intersection hostscements with temperatures of 13 to 88 °C. The spatial pattern of cement temperaturesrevealed by clumped isotope thermometry suggests that intensely jointed zonesassociated with fault intersections enable rapid down-fault migration of cool surfacewaters and that deformation-band faults with their associated slip surfaces may furthercompartmentalize fluid flow, restricting fluid sources to warm waters thermally equili-brated with the country rock outside the jointed zone. Our data confirm that therelationship between faults and fluid flow can vary greatly over short length scales, andsuggest that some fracture zones can be highly conductive to depths as great as 2 km.

Key words: Deformation structures, diagenesis, fluids, calcite cement, fault, Para-dox Basin, clumped isotopes

introductionBrittle fault systems can serve as either conduits or barriers to fluid flow (for

example, Caine and others, 1996; Davatzes and others, 2005), impacting mass and heattransfer in the crust and influencing the potential storage and migration of hydrocar-bons and geothermal fluids. For fault systems in porous sandstones, two classes ofstructures control both hydrological and mechanical behavior during fault evolution:cataclastic deformation bands and joints. Deformation bands form tabular and anasto-mosing zones of localized deformation and crushed grains (Aydin and Johnson, 1978)and may evolve to host discrete slip surfaces (Aydin and Johnson, 1978; Fossen andothers, 2007). Joints are planar fractures that show displacement normal to theirsurfaces and may experience subsequent shear that leads to brecciation (for example,Myers and Aydin, 2004; Davatzes and others, 2005). While deformation bands andsubsequent slip surfaces typically reduce permeability within and across fault zones(Antonellini and Aydin, 1994), joints can act as significant conduits for fluid (forexample, Long and others, 1996; Aydin, 2000).

† Corresponding author: [email protected]

[American Journal of Science, Vol. 313, May, 2013, P. 490–515, DOI 10.2475/05.2013.03]

490

The development of these structures during faulting in sandstones and theirinfluence on fluid migration has been studied in detail along the Moab Fault, a largenormal fault system in the Paradox Basin, Utah (Nuccio and Condon, 1996; Foxfordand others, 1996, 1998; Chan and others, 2000; Davatzes and others, 2003, 2005;Johansen and others, 2005, 2008; Eichhubl and others, 2009). Recent work highlightsthe importance of both structures and diagenesis in controlling fluid migration in thisand other large fault systems (Eichhubl and others, 2000, 2004, 2009; Davatzes andothers, 2005; Fossen and others, 2005; Laubach and Ward, 2006; Laubach and others,2009). Diagenetic cements precipitated along the Moab Fault preserve informationabout the origin and history of the diagenetic fluids from which they grew, and theirabundance in areas of structural complexity led previous workers to infer thatpaleo-fluid flow was focused along highly jointed fault segments (Eichhubl and others,2009).

These mapping results combined with fluid inclusion micro-thermometry andstable isotopic analysis of calcite cements from the Moab Fault suggest that jointsserved as conduits for the ascension of warm, saline basinal fluids that interacted with ashallower meteoric water source (Chan and others, 2000; Eichhubl and others, 2009).Chan and others (2000) envisioned this shallower, 18O and 13C-enriched end-memberto be sourced from high-elevation meteoric precipitation, driven by topographicgradients to circulate deep in the basin, where it interacted with hydrocarbons fromdeeper stratigraphic levels to precipitate calcite cement at temperatures on the orderof 50 or 25 °C. Subsequently, Eichhubl and others (2009) observed primary two-phasefluid inclusions from one sample indicating calcite cement growth temperatures of 84to 125 °C. They interpreted these values to be consistent with topographically driven,deep circulation of meteoric water, with the higher range of temperatures represent-ing focused flow of hot fluid up the fault zone, but lacked the data to investigate therelationship between fluid temperature and distance from the fault.

We complement previous work by using clumped isotope thermometry (Ghoshand others, 2006; Eiler, 2007) to document spatial variations in the temperature of thefluids from which calcite cements precipitated. Huntington and others (2011) usedclumped isotopes to independently determine both the temperature and oxygenisotopic composition of the water (�18OH2O) from which diagenetic cements from theColorado Plateau grew, and Swanson and others (2012) applied the method to studyconditions of cataclastic deformation along the Mormon Peak detachment in the Basinand Range, Nevada. We apply this technique for the first time to study the role of faultzone heterogeneity in controlling fluid flow in the shallow crust. Along joint-dominated fault segment 5 (fig. 1), we find high temperature cements, consistent withprevious fluid inclusion microthermometry estimates and structural analysis indicatingthat the fault was a conduit for hot fluids (Eichhubl and others, 2009). However, nearthe intersection of fault segments 1 and 2—a zone characterized by both deformationbands and slip surfaces and abundant joints—we find a broad range of temperaturesthat vary systematically with distance from the fault and correlate with variations insecondary deformation structures, providing further evidence that these structuresplay an important role in transmission and compartmentalization of fluids in porousrocks.

study areaThe Moab Fault is a basin-scale normal fault cutting Pennsylvanian to Cretaceous

sedimentary units in the Paradox Basin of the southwestern United States (fig. 1;Doelling, 1985; Foxford and others, 1996; Nuccio and Condon, 1996; Davatzes andAydin, 2003; Davatzes and others, 2005). The Moab Fault was active between thePermian and mid-Tertiary, and the last significant fault motion has been dated at 50 to60 Ma from K-Ar dates in fault zone illite, indicating faulting occurred near maximum

491S. C. Bergman, K. W. Huntington, & J. G. Crider 491

burial (Pevear and others, 1997). Both the structural evolution and diagenetic historyof the Moab Fault system have been studied extensively (for example, Foxford andothers, 1996, 1998; Pevear and others, 1997; Garden and others, 2001; Davatzes andAydin, 2003; Davatzes and others, 2003, 2005; Johansen and others, 2005, 2008; Solumand others, 2005, 2010; Eichhubl and others, 2009). Our work builds on highresolution prior mapping (Davatzes and others, 2005; Johansen and others, 2005;Eichhubl and others, 2009) to examine the relationship between structural architec-ture and fault permeability with new paleotemperature determinations from clumpedisotope thermometry.

We analyzed calcite fault cements at Courthouse Rock, near Moab, Utah, at theintersection of the through-going southern section of the Moab Fault (fault segment 1,fig. 1) and the northern section, which comprises a series of hard-linked, northwest-trending fault segments (fault segments 2-5, fig. 1; Doelling, 1985, 2002; also known asthe Courthouse Fault; Fossen and others, 2005). High-resolution structural mappingby two independent groups has shown that fault segments are constructed from andassociated with cataclastic deformation bands, slip surfaces, and joints (Davatzes andothers, 2003, 2005; Johansen and others, 2005). Johansen and others (2005) observedtwo classes of deformation bands at Courthouse Rock: “thick” deformation bands thatweather in positive relief, host moderate grain size reduction, and form zones severalcentimeters wide; and “thin” deformation bands characterized by intense comminu-tion in a bleached zone tenths of millimeters wide. Thin deformation bands and jointsare difficult to distinguish at the outcrop. These two styles of fracture, with or withoutsubsequent slip surfaces, are observed to consistently overprint wide zones of “thick”deformation bands (Davatzes and others, 2003, 2005; Johansen and others, 2005), andthere is some evidence that joints may also post-date the “thin” deformation bands

Quaternary Deposits (Q)

Upper Jurassic units (Jmb, Jms, Jmt)

Moab Sandstone (Jctm)

Middle Jurassic units (Jes, Jc, Jcd)

Navajo Sandstone (Jn)

Cretaceous sandstones (Kd+cm)

Fault

Sampling siteA

Fault segment1

JmbJmb

Q

Q

QQ

Q

Q

Kd+cm

Kd+cm

Jms

Jms Jms

QJmt

Jmt

Jmt

Jctm

Jctm

Jctm

Jctm

Jes

Jes Jes

Jes

Jcd JcdJcd

Jcd

Jc

Jc

JnJn

1

2a

5

38º4

2’30

’’N

109º45’W 109º40’W 109º35’W

200 m

NA

B

C

Figure 2 Utah

Fig. 1. (A) Geologic map of the Moab Fault system at Courthouse Rock redrawn and simplified fromDavatzes and others (2005), and Eichhubl and others (2009). Fault segments referenced in the text arenumbered following Davatzes and others (2005). Sampling sites are indicated by white stars. Unit symbols asfollows: Kd � cm: Cretaceous Dakota and Cedar Mountain Formations, undifferentiated; Jmb, Jms, and Jmt:Brushy Basin, Salt Wash, and Tidwell Members of the Jurassic Morrison Formation; Jc, Jctm: Jurassic CurtisFormation and Moab Tongue Members; Jes: Slick Rock Member of the Jurassic Entrada Formation; Jcd:Dewey Bridge Member of the Jurassic Carmel Formation. Inset shows the approximate location of the studyregion in eastern Utah.

492 S. C. Bergman, K. W. Huntington, & J. G. Crider—Tracing paleofluid sources

(Johansen and others, 2005). Quartz diagenesis variably reduced the primary porosityof sandstone at Courthouse Rock at early stages of deformation and likely influencedsubsequent mechanical behavior of the rock (Johansen and others, 2005). Deforma-tion intensity increases in areas of complex fault geometry, such as at the intersectionof fault segments 1 and 2a (Davatzes and others, 2003, 2005; Johansen and others,2005). At these intersections, fractures are filled with calcite cements, which are foundprimarily as veins and concretions along fault segment 2a in the Moab Member of theCurtis Formation (formerly mapped as the Moab Member of the Entrada Sandstone),and along fault segment 5 in the Navajo Sandstone (mapping and analysis by Eichhubland others, 2009). Carbonate cement is absent in areas of the fault characterized byzones of “thick” deformation bands that are not overprinted, suggesting that localfractures occurring at intersections between segments of the Moab Fault acted aspreferred fluid conduits (Foxford and others, 1996; Davatzes and others, 2005;Eichhubl and others, 2009).

sample collection and characterization

We sampled fault-related calcite for clumped isotope thermometry and traceelement geochemistry from three sites along and near fault segments near CourthouseRock (fig. 1). The sampled calcite occurs as veins and associated 2- to 3-cm-thick halosof pore-filling calcite cement surrounding veins (Eichhubl and others, 2009). Site Asamples were collected immediately adjacent to fault segment 5 in the Navajo Sand-stone (N38°42�25�, W109°44�15�; fig. 1). Site B samples were collected near theintersection of fault segments 1 and 2a along a transect running perpendicular to faultsegment 2a and from additional locations in the Moab Member of the Curtis Forma-tion (figs. 1 and 2). Two additional samples were collected at site C (N38°42.5�,W109°44.6�) from the Moab Member of the Curtis Formation in Mill canyon, approxi-

N

Q

Q

Q

2'

B

1

2a

Jctm

1

2'

JctmJmt

2a

A

Q

Q

Jmt

Jes

Jctm

Jmt

Jcd

Q

Jmb

Kd+cm N

meters 500

11

1819

20

2224

2526

13

09

0708

15

16

09

10SB sample

11SB sample

Carbonate cementFault Segment1

Joint

Deformation band-dominated fault

Joint-dominated fault

Sample transect

Fig. 2. (A) Geologic map of sampling site B at the intersection of fault segments 1 and 2a (CourthouseJunction), redrawn and simplified from Eichhubl and others (2009). Unit symbols as in figure 1. (A) Samplelocations (see table 1). (B) Structural and diagenetic map of sampling site B, with joints as mapped byDavatzes and others (2005) and distribution of calcite cement generalized from Eichhubl and others (2009).See also Johansen and others (2005).

493using clumped isotope thermometry of diagenetic cements along the Moab Fault, Utah

mately 1 km west of Site B, near the intersection of fault segments 2 and 3 (fig. 1; seeDavatzes and others, 2005).

Millimeter-to-centimeter length prismatic calcite crystals with abundant fluidinclusions fill cm-to-dm wide joints sampled at site A. In contrast, joints at site B aremm-to-cm wide, filled with mm-to-cm length, flat, white, fibrous calcite crystals. At siteC mm-to-cm length, fibrous calcite crystals fill mm-to-cm wide joints. Minor bitumenwas found at both sites A and B. Malachite also occurs at sites B and C and is thought tobe the most recent cement phase at Courthouse Rock (Eichhubl and others, 2009).

Samples were characterized in thin section with transmitted and polarized lightand cold-cathode cathodoluminescence (CL) microscopy, the latter performed usinga Technosyn Luminoscope operated at 8 –10 kV, 0.5 mA, and 6.7–9.3 Pa to examinethe textures of fault cement calcite and to help constrain the origin of diageneticfluids. Minerals luminesce based on the abundance of trace elements in the crystallattice, and calcite luminescence, which commonly appears yellow-orange to red,is typically activated by Mn2� ions and quenched by Fe2� ions (Boggs and Krinsley,2006). At Courthouse Rock, cements within �500 m of one another display markedlydifferent luminescence patterns and crystal morphologies (figs. 3 and 4). Given theamount of material needed for precise clumped isotope thermometry (�8-12 mg) andtrace-element analysis (2-5 mg), some samples contain both vein and halo material,while others contain only vein material (see table 1).

clumped isotope analysis and resultsCalcite samples were removed from hand samples by drilling or plucking and

powdered with an agate mortar and pestle. For four of the samples, long, prismaticcalcite crystals were subdivided into two to three sections parallel to the growthdirection prior to powdering to examine possible temperature changes through time(table 1). Previous work indicates no measurable effect on clumped isotope analysisdue to these different sampling methods (Swanson and others, 2012).

Clumped isotope samples were pre-treated by soaking in 3 percent H2O2 for 45minutes, followed by rinsing in deionized water and freeze-drying to remove organicmaterial (see table 1 for exceptions). Pre-treating internal lab standards using H2O2does not affect conventional stable isotope or clumped isotope measurements (Tripatiand others, 2010). All samples were analyzed at the California Institute of Technologyfollowing the methods of Passey and others (2010), described here briefly. CO2samples were produced from 8 to 12 mg of calcite reacted in a common acid bath(104% H3PO4) at 90 °C for 10 minutes. Product CO2 was separated from evolved H2Ovia passage through multiple cryogenic traps. The CO2 analyte was then entrained inHe carrier gas and passed through a Poropak Q column in a gas chromatograph heldat �20 °C. Purified CO2 was analyzed on a ThermoFinnigan MAT 253 mass spectrom-eter configured to measure m/z ratios for masses 44 to 49 and screened for mass-48contaminants. We report �47 values both in the Caltech reference frame (all �47 valuesnormalized to stochastic �47 values and corrected for linearity and scale compressionusing heated gases; Huntington and others, 2009) and in the absolute reference frame(ARF; Dennis and others, 2011). The transfer function from the Caltech referenceframe to the ARF was calculated using a secondary standardization, using assumed �47values for 1000 °C heated gases and carbonate standards (Carrara marble, TV-01calcite, and Carmel calcite; see Appendix A for data and details of transfer functioncalculations). These �47 values along with measured �13C and �18O values (referencedto VPDB) are presented in table 1.

Calcite growth temperature [T(�47)] was calculated in three ways: (1) usingCaltech reference frame �47 values and the theoretical calcite clumping-temperatureequation of Guo and others (2009), which couples a theoretical model of 13C-18Oclumping (Schauble and others, 2006) with predicted kinetic isotope effects from


phosphoric acid digestion of carbonate; (2) using ARF �47 values and the empiricalcalibration of Ghosh and others (2006) transferred to the ARF by Dennis and others(2011); and (3) using ARF �47 values and the empirical calibration of Dennis andSchrag (2010) transferred to the ARF by Dennis and others (2011). Temperaturescalculated using all three methods are listed in table 1. Although choice of reference

10SB201 mm

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10SB20

11SB05

11SB07

A

B

C

Fig. 3. CL photomicrographs of samples from site A. (A) CL image for sample 11SB05 (91-100 °C),characterized by bright orange luminescence, zoning defined by variations in calcite luminescence andcalcite twinning (see arrows); scale bar represents 2 mm. (B) CL image for sample 11SB07 (67-95 °C),characterized by quartz diminution and calcite vein fracture; scale bar represents 2 mm. (C) CL image forsample 10SB20 (128 °C), characterized by zoning defined by variations in calcite luminescence, andextremely bright orange luminescence; scale bar represents 1 mm. See text for further description.


frame and calibration does not significantly impact our interpretations, because theGuo and others (2009) equation has not been transferred to the absolute referenceframe and the calibration data of Ghosh and others (2006) extend only from 0 to

11SB19

A

10SB09 11SB16

B

10SB08 10SB15

11SB25 10SB13

C

Fig. 4. CL photomicrographs of samples from site B; all scale bars represent 2 mm. (A) CL image forsample 11SB19 (29 °C), characterized by weak to non-luminescent brown calcite cement. (B) CL images forsamples 10SB09 (50 °C) and 11SB16 (42 °C), characterized by calcite twinning, calcite vein fracture, andoccasional zoning in calcite luminescence, see arrows. (C) CL images for samples 10SB08 (60 °C), 10SB15(65 °C), 11SB25 (71-73 °C), and 10SB13 (71 °C); characterized by variable orange to orange-red lumines-cence, calcite twinning, quartz diminution, and zoning in calcite luminescence as described further in thetext.


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50 °C, we limit our discussion in the text to calcite temperatures calculated usingmethod (3; “ARF, D&S”). We calculated �18OH2O values (referenced to VSMOW) fromT(�47) and measured �18Ocarb using the calcite-water fractionation factor of Kim andO’Neil (1997). We discuss �18OH2O values derived from T(�47) (ARF, D&S) in the textand figures, and we provide �18OH2O values derived from T(�47) (ARF, Ghosh) in table1 for reference; note that �18OH2O values derived from T(�47) (Caltech, Guo) fallbetween these values.

Samples were analyzed one to three times, with average values of �47 ranging from0.517 to 0.734 permil (ARF) and T(�47) values corresponding to calcite growthtemperatures of 13 to 128 °C (ARF, D&S). The �47 values for samples representingdifferent stages of growth in the same crystal (indicated with a, b, c in sample name,where “c” represents later growth; table 1) agree within analytical error (1 SE) forsamples 11SB05, 11SB18, and 11SB25 (average temperatures of 96 5 °C, 17 2 °C,and 72 1 °C (1 SD), respectively). While �47 values for samples 11SB07a and11SB07b are within 1 SE (average temperature 90 6 °C, 1 SD); the �47 value for11SB07c is 1 SE higher, corresponding to a temperature of 67 °C. Sample averagevalues for �18Ocarb range from �22.3 to �8.5 permil, and values for �13C range from�6.27 to 1.07 permil, with average precisions for externally replicated samples of 0.1permil and 0.06 permil, respectively (1 SE). Calculated �18OH2O values range from�13.2 to �2.9 permil (table 1).

trace element analysis and resultsA subset of the calcite samples from sites A and B was prepared for trace element

analysis via inductively coupled argon plasma optical emission spectroscopy (ICP-OES)at the University of Washington. Powdered calcite in 2 to 5 mg aliquots was reacted in 3mL of nitric acid for 10 minutes to dissolve the solid CaCO3. Each CaCO3OHNO3solution was then diluted by volume to 50 mL and analyzed on a Perkin-Elmer 3300DV.ICP-OES trace element analyses were performed in an attempt to further constrainvariability in the origin of the fluids from which samples at and within sites A and Bprecipitated; the results show only minor variation in Ba/Ca and Sr/Ca ratios amongsamples from sites A and B, with most measured values being below the detection limitof 0.1 ppb (table 2).

discussionOur T(�47) results confirm previous observations that carbonate cements along

the Moab Fault precipitated from multiple fluids (Chan and others, 2000; Eichhubl

Table 2

ICP-OES results

Sample Ba/Ca

(ppb)

Sr/Ca

(ppb)

Ba

(ppb)

Sr

(ppb)

Ca

(ppm)

Site A, Navajo Sandstone at fault segment5

11SB07

11SB05

<0.1

<0.1

1.7

2.5

<0.1

<0.1

33.7

77.4

20.0

31.4

Site B, Moab Member of Curtis Formation at Courthouse Rock

11SB09

11SB16

11SB19

11SB24

11SB25

11SB26

0.1

<0.1

<0.1

<0.1

<0.1

0.1

0.6

1.0

0.8

1.3

0.8

0.9

2.1

<0.1

<0.1

0.1

2.0

2.3

10.9

8.8

4.8

33.0

20.5

16.3

17.1

9.1

6.1

25.1

24.1

17.9


and others, 2009), and provide new evidence that cement growth occurred over a widerange of temperatures that varied spatially at the meter-scale. Although for simplicitythe following sections present calcite temperatures calculated using the absolutereference frame and Dennis and Schrag (2010) calibration, our conclusions areinsensitive to the choice of reference frame or calibration (table 1; figs. 5-7).

Constraints on Fluid Flow and Cementation at Site ABased on previous stable isotopic analyses, fluid inclusion work, and basin history

models, we anticipated that cements associated with fault segment 5 (site A; fig. 1)precipitated from volumetrically minor basinal fluids mixing with meteoric water,during or closely following maximum burial of the Moab Member following mid-Cenozoic faulting (Nuccio and Condon, 1996; Chan and others, 2000; Garden andothers, 2001; Eichhubl and others, 2009). Therefore, we expected cement tempera-tures and isotopic compositions at site A to reflect calcite precipitation from meteoricwaters at temperatures near those of the host rock (Navajo Sandstone) at maximumburial depth of �2 km (�80-100 °C; Nuccio and Condon, 1996; Vrolijk and van derPluijm, 1999; Garden and others, 2001).

Our T(�47) data from site A are consistent with this hypothesis, clustering around70 to 100 °C for vein calcite samples (11SB05a, b, c and 11SB07a, b, c) and ranging upto 128 °C for one sample (10SB20) containing both vein and halo calcite. Calcite insample 10SB20 occurs as pore-filling cement that exhibits zoning defined by variationsin luminescence, which suggests growth over an extended period of time withchanging fluid trace element composition (fig. 3C). Calcite zones in this sample are

80

Distance from Fault Segment 2a (m)

20

40

60

100

120

0 20 40 60 80 100 1200

T(Δ

47) (º

C)

Faul

t Seg

men

t 2’

-13.2 to -11.1 ‰-11.0 to -9.1 ‰-9.0 to -7.0 ‰

δ18OH2O ARF, Dennis & Schrag, 2010ARF, Ghosh et al., 2006

T(Δ47): (VSMOW):

Fig. 5. Distance along the sample transect north of fault segment 2a versus T(�47) for samples from siteB. Symbol shading indicates the oxygen isotopic composition of the fluid from which the cementprecipitated (�18OH2O, VSMOW‰, ARF, D&S). Large circles indicate T(�47) calculated from �47 values inthe absolute reference frame and temperature calibration of Dennis and Schrag (2010), as discussed in text.Small gray circles connected to these large circles indicate T(�47) for the same sample calculated from �47values in the absolute reference frame and temperature calibration of Ghosh and others (2006), forreference.


commonly bright orange, red, or dark red luminescent to non-luminescent, and wherebright orange luminescent cement is present, it is commonly the earliest phase ofgrowth at the center of calcite crystals (fig. 3C). Sample 10SB20 also contains bitumen,suggesting that the cement precipitated from a fluid that interacted with hydrocar-bons. For the cooler samples, sample 11SB05 shows zoning in calcite crystals defined bybright orange to yellow luminescence, as well as pervasive calcite twinning (fig. 3A).Sample 11SB07 shows the same bright orange to yellow luminescence as 11SB05, but it

Fig. 6. Calculated �18OH2O versus T(�47) values for all samples at sites A, B, and C. Error bars are smallerthan symbol size. There is no correlation between fluid isotopic composition and calcite precipitationtemperature, indicating diagenetic cements precipitated from fluids with a range of oxygen isotopic com-positions over a wide range of temperatures as discussed in the text. (A) T(�47) and �18OH2O valuescalculated from �47 values in the absolute reference frame and the temperature calibration of Dennis andSchrag (2010). (B) T(�47) and �18OH2O values calculated from �47 values in the Caltech reference frame andthe temperature calibration of Ghosh and others (2006).


exhibits only minor zoning defined by variations in calcite luminescence and calcitetwinning (fig. 3B). Although all samples from site A precipitated at elevated tempera-tures, the variability in T(�47) and in calcite luminescence at site A suggest thatdifferent temperature calcites precipitated from different fluid sources at differenttimes.

The range of observed fluid inclusion homogenization temperatures (TH �84-125 °C) for the calcite sample from site A analyzed by Eichhubl and others (2009)

−6 −4 −2 0 20

20

40

60

80

100

120

140

site Asite Csite B

−6 −4 −2 0 20

20

40

60

80

100

120

140

T(Δ

47) (º

C),

AR

F, D

&S

T(

Δ47

) (ºC

), A

RF,

Gho

sh

site Asite Csite B

δ13Ccarb (‰, VPDB)

δ13Ccarb (‰, VPDB)

(B)

(A)

Fig. 7. Measured �13C versus T(�47) values for all samples at sites A, B, and C. Error bars for �13C aresmaller than symbol size. Cement temperature and carbon isotopic composition are correlated at site B (r2 �0.65) and across the study area (r2 � 0.67), indicating changes in the carbon pool with changing calciteprecipitation temperature, and therefore changing diagenetic fluid source. (A) T(�47) calculated from �47values in the absolute reference frame and the temperature calibration of Dennis and Schrag (2010). (B)T(�47) calculated from �47 values in the Caltech reference frame and the temperature calibration of Ghoshand others (2006).


overlaps with the range of clumped isotope temperatures. Eichhubl and others (2009)suggest that cements with temperatures greater than �100 °C likely precipitated fromminor pulses of hot basinal fluids ascending the Moab Fault. Sample 10SB20 (128 °C),which exhibits a distinctive luminescence pattern (fig. 3C), may represent precipita-tion from one such pulse of hot basinal fluids.

The oxygen and carbon isotopic compositions of calcite cements from site A arealso consistent with the hypothesis that the cements precipitated from deeply circulat-ing meteoric waters. Calculated �18OH2O values for waters in equilibrium with site Acements range from �10 to �3 permil, enriched in 18O with respect to modernmeteoric waters in the Paradox Basin (�15 to �12‰ VSMOW; Spangler and others,1996) (table 1). This enrichment in 18O could be attributed to a variety of factorsincluding climate change, evaporative enrichment at the surface, or subsurfaceinteractions between waters and host rocks. Carbon isotopic values for site A veincalcites (�6.3 to �4.4‰) are slightly depleted in 13C relative to local limestones (�1to �4‰ VPDB; Garden and others, 2001), but significantly more enriched in 13C thanmethanogenic carbonates (�30 to �40‰ VPDB; Boles and others, 2004; Eichhubland others, 2009). The intermediate carbon compositions at site A and association ofbitumen with calcite veins observed by us and previous workers at fault segment 5(Eichhubl and others, 2009) indicate that calcite cements precipitated from fluids thatscavenged bicarbonate from local limestones, groundwater, and residual hydrocar-bons.

Constraints on Fluid Flow and Cementation at Site BSite B (Courthouse Rock) is located 500 m northwest of site A, where the

structural architecture is defined by both deformation bands and intense secondaryfracturing at a fault intersection (Davatzes and others, 2005; Johansen and others,2005). The site is divided grossly into two domains by a second-order, deformation-band fault (labeled 2� in fig. 2).

Our new carbon and oxygen isotopic data from site B within 30 m of fault segment2a are consistent with previously published isotopic data that suggest a dominantlymeteoric source for fluids from which the cements precipitated; however, the �18O and�13C values of calcite we collected on a transect perpendicular to the fault segmentsuggest systematic spatial variations in diagenetic fluid sources and calcite cementa-tion. While both our calcite �13C data and the data of Eichhubl and others (2009)range from �3.5 to �1.3 permil VPDB between fault segments 2a and 2�, our new datafor cements north of fault segment 2� all plot near 3 permil, suggesting a change in thecarbon pool from which the cements were sourced (fig. 8). In addition, our dataindicate calcite �18O and �13C values are correlated, with �18Ocarb values varying from�19 to �9 permil VPDB between fault segments 2a and 2� and clustering around �19permil north of segment 2� (fig. 9), suggesting spatial heterogeneity of diagenetic fluidsources and calcite cementation.

The T(�47) data show that the temperature of the diagenetic fluids from whichcalcite cements grew also varied considerably over distances of tens of meters (fig. 5).Clumped isotope temperatures for cement samples collected north of fault segment 2�range from 51 to 84 °C, overlapping the range of temperatures observed at site A.However, cements in the zone of abundant fracturing between fault segments 2 and 2�range from 13 to 88 °C. The lowest temperatures in this range are too cool to recordcalcite precipitation from fluids thermally equilibrated with the host rock nearmaximum burial of the host sandstone, further suggesting multiple fluid sources.

Constraints on Fluid Flow and Cementation at Site CSite C is located at the intersection of fault segments 2b, 2c and 3 (mapped by

Davatzes and others, 2005; Eichhubl and others, 2009) and is characterized by both


joints and deformation bands. We present T(�47) data for two cement samples fromsite C. The first sample at site C yields a T(�47) value of 95 °C; this result is similar toaverage temperatures at site A and the highest temperatures at site B, and is consistentwith estimated temperatures of the country rock during maximum burial. The secondsample at this site yields a T(�47) value of 47 °C, which is within the range of

Distance from Fault Segment 2a (m)

Fault Segm

ent 2’

−25

−20

−15

−10

−5

δ18O

carb V

PD

B ‰

0 20 40 60 80 100 120

Fig. 9. Distance along the sample transect north of fault segment 2a versus �18Ocarb for samples fromsite B. Analytical uncertainty is smaller than the symbol size. The greatest variation in the oxygen isotopiccomposition of calcite cements occurs in the heavily jointed region between fault segments 2a and 2�. Basedon �18Ocarb data alone it is not possible to determine if the variation reflects variation in fluid temperature,isotopic composition, or both.

-4

-3

-2

-1

0

1

2

0 20 40 60 80 100 120 Distance from Fault Segment 2a

δ13C

VP

DB

‰

Faul

t seg

men

t 2'

Fig. 8. Distance along the sample transect north of fault segment 2a versus �13C for samples from site B.The greatest variation in carbon composition occurs in the heavily jointed region between fault segments 2aand 2� (0-30 m on the figure, see fig. 2B). Analytical uncertainty (1 SE) in �13C and distance is smaller thanthe symbol size.


temperatures observed for cements collected within 30 m of fault segment 2 at site B,and is significantly cooler than expected for fluids ascending the fault or in theadjacent host rock following deformation near maximum burial. These samples ploton the �13C versus T(�47) trend defined by the site A and B samples (fig. 7).

Hypotheses for the Origin of Low-Temperature CementsWhile warm cement temperatures can be explained by a fluid-cementation regime

described by meteoric groundwaters at ambient geothermal temperatures interactingwith a deeper basin source (for example, Chan and others, 2000; Eichhubl and others,2009), a fundamentally different regime varying in time and/or space must be invokedto explain how some carbonate cements formed at temperatures consistent withEarth-surface conditions. We propose two end-member scenarios that could explainprecipitation of the low-temperature cements at sites B and C: the cements could havegrown from either 1) fluids traveling through fractures from the surface to depthsufficiently rapidly that calcite precipitated before the fluids thermally equilibratedwith the host rock, or 2) fluids thermally equilibrated with the host rock when it wasnear the surface.

Scenario 1 invokes highly conductive joints to enable rapid downward migrationof surficial fluids and low-temperature cement growth at depth. This hypothesispredicts that the coolest cements precipitate at fault intersections where fracturedensity is observed to be greatest (Davatzes and others, 2005; Johansen and others,2005; Eichhubl and others, 2009), and the greatest quantity of surface water might beexpected to rapidly infiltrate the fault. Cements farther from the main fault segmentsmight record warmer temperatures, reflecting the warming of surface fluids as theymigrated away from this conduit through the warm host sandstone at depth. Thus, thisscenario predicts that the spatial distribution of cool cements is limited to regions offracturing adjacent to faults. Migration of cool surficial fluids away from the faultwould be inhibited by low permeability zones of deformation-band faults and associ-ated slip surfaces. Scenario 1 does not predict relative timing of cool and warmcements.

Scenario 2 proposes that the cool clumped isotope temperatures represent calcitegrowth near the Earth’s surface, late in the exhumation history of the Basin. Thisscenario predicts the relative ages of warm and cool carbonate cements: early calciteprecipitated at elevated temperatures from upward migrating fluids, while latercements precipitated throughout exhumation of the host sandstone. Scenario 2 doesnot require cool cements to be restricted to near-fault fractures.

In both scenarios, we expect cements with meteoric water signatures, althoughhigher-temperature calcite samples might be enriched in 18O and depleted in 13C dueto interaction with silicate rocks and residual hydrocarbons at depth. At all three sites,calculated values of �18OH2O in equilibrium with the calcites suggest a dominantlymeteoric source with variable contribution from basinal waters enriched in 18O.Although �18OH2O values and T(�47) are not strongly correlated (fig. 6) and thus donot provide insight in to the source(s) of warm versus cooler fluids, calcite �13C valuesat site B vary with distance from fault segment 2a and are highly correlated with T(�47)(R2 � 0.65), indicating that the cooler cements reflect a carbon source more enrichedin 13C (�13C approximately �2 to 1‰) than the warmer cements (�13C approximately�4 to �3‰). These warmer cements approach the carbon isotopic compositions forcalcites at site A, which we infer to have precipitated from fluids migrating upwardalong the fault as previously suggested by Eichhubl and others (2009).

Systematic variability in calcite luminescence observed at site B also supports thenotion that the different temperature cements precipitated from multiple fluidsources (fig. 4). Calcite cement in sample 11SB19, which precipitated at low tempera-ture (29 °C), is non-luminescent to weakly luminescent brownish orange and lacks


twinning or zoning (fig. 4A). In contrast, the higher temperature samples (between 42and 50 °C) we examined show orange to bright orange luminescence, extensive calcitetwinning, occasional zoning, and fractured calcite crystals within veins (fig. 4B).Although the luminescence of the warmer (60-73 °C) cements at site B is variable,showing weak to bright luminescence in orange, reddish-orange and yellow (fig. 4C),these cements commonly exhibit luminescence that is darker in color (more reddish-orange than yellow-orange) compared to the 42 to 50 °C cements. Zoning defined byvariations in calcite luminescence, calcite twinning, and occasional quartz diminutioncharacterize the high temperature samples.

To evaluate the relative timing of warm versus cool cements, we measured T(�47)variation within single calcite crystals. If the cool cements grew exclusively from cool,shallow groundwaters following significant exhumation of the host sandstone (sce-nario 2), we expect cement temperatures to decrease with time. Three sub-sampledcalcite crystals from sites A and B have �47 values for different aliquots of the samecrystal that agree within 1 SE, and therefore these samples do not show significantcooling through time (11SB05a,b,c; 11SB18a,b,c and 11SB25a,c; table 1). For sample11SB07 from site A, �47 values for subsamples a and b show no variation in tempera-ture, and although the �47 value for subsample c is more than 1 SE higher than theother aliquots of calcite taken from the same crystal, the �47 values for all subsamplesof 11SB07 agree within 2 SE. Thus the data do not support significant cooling of thefluid during crystal growth and are not cool enough to represent Earth-surfacetemperatures. However, since the timing of crystal growth is unknown, the absence ofcooling during crystal growth does not rule out near-surface cement growth from coolgroundwater. No other samples provide constraints on the relative timing of low- andhigh-temperature cements.

The fault-normal transect at site B illustrates the spatial variability in the tempera-ture of carbonate cements (fig. 5). While the warmest (64-88 °C) cements are foundassociated with veins and concretions at distances of 3 to 109 m from fault segment 2a,cool (13-27 °C) carbonate cements are limited to the highly-fractured region betweenfault segments 2a and 2� (fig. 2). The variability in �18OH2O and �13C values is similarlyreduced across segment 2� (figs. 8 and 9). This pattern suggests that deformationband-dominated fault segment 2� may have acted as a baffle against lateral flow oflow-temperature fluids, arguing for rapid penetration of surface waters flowing downthe high-permeability zone around 2a (scenario 1). If cool fluids infiltrated the hostrock only following significant exhumation when the host sandstone was near thesurface (scenario 2), low-temperature calcite would be expected throughout given thepresence of fractures on either side of 2� (fig. 2). Similar to site B, site C, which alsohosts both cool and warm cements, is a structurally complex fault interaction zone(Davatzes and others, 2005), further supporting the inference that secondary fractur-ing controls the spatial distribution of cool cements.

Is it reasonable to infer that cold surface waters could reach depths of 2 kmwithout warming? We can address this problem by evaluating the thermal Pecletnumber (Pe), a dimensionless value that represents the contribution of advectiveversus conductive heating. Following Ingebritsen and others (2006): Pe � qwcw�wL/Krock ; where qw, cw, and �w are the flow rate, heat capacity, and density of the fluid, Krockis the thermal conductivity of the host rock and L is a characteristic length scale. WhenPe � 1, conduction dominates and fluid temperature is equilibrated with the rock;when Pe 5, the system is essential isothermal, dominated by advection, and con-trolled by the source-fluid temperature. Over a length scale of 10 km, assuming fixedtemperature boundaries, a standard geothermal gradient (25 °C/km), standard physi-cal properties for water and rock (cw � 4.2 kJ/kg/°C; �w � 103 kg/m3; Krock � 2W/m/°C), cool water can reach 2 km depth at moderate flow rates of 10�10 m/s.


These values give a Peclet number of 2, of the same order as observations fromhydrological experiments in fracture-dominated flow (Anderson, 2005, and referencestherein).

Based on our observations from calcite cements at sites A, B, and C, it appears thatinteraction of meteoric groundwater and a deeper basinal source led to calcitecementation throughout the study area, while down-going surface waters penetratedrapidly to significant depth only at fault intersection zones where fracture density isgreater. These clumped isotope data provide new insight into fluid sources andpathways controlled by structural complexity, and combined with carbon and oxygenisotopic data, CL microscopy, and other observations of previous workers are consis-tent with findings that the structural architecture influences fluid flow and cementa-tion in this area (Eichhubl and others, 2009).

conclusionsClumped isotope thermometry along the Moab Fault at Courthouse Rock show

that calcite veins precipitated from meteoric waters over a wide range of temperatures(13-128 °C). Our work provides evidence for carbonate growth from Earth surface-temperature fluids along the Moab Fault and suggests that the Fault served as a conduitfor both ascending and descending fluids. This study area is characterized by fault zoneheterogeneity, with faults formed from both deformation bands and joints. Our resultssupport earlier findings that interactions between these two classes of structuresdetermined where fluids migrated at Courthouse Rock. The spatial distribution oflow-temperature cements argues for rapid penetration of surface waters flowing downintensely-fractured fault intersections, and suggests that deformation-band faults servedas low-permeability baffles, preventing lateral migration of cold fluids. Thus, it appearsthat structural heterogeneity is responsible for cement precipitation over a wide rangeof temperatures prior to exhumation of the host rock. Carbonate clumped isotopethermometry quantified calcite growth temperatures below �30 °C and the spatialpattern of cement temperatures, and it is only these new data that made ourinterpretation possible. Our study suggests this new technique permits evaluation ofthe role of these important structures in influencing fluid flow in ancient fault systems.

acknowledgmentsAcknowledgment is made to the donors of the American Chemical Society

Petroleum Research Fund for support of this research (ACS-PRF grant 49709 and NSFgrant EAR-115613 to KWH). We thank the donors of the University of Washington,Department of Earth and Space Sciences for support of this research (GeorgeGoodspeed Fellowship and Dorothy G. Stephens Fellowship to SCB). We thank JohnEiler, Nami Kitchen and Ron Sletten for generous laboratory access and assistance. Wethank Gerd Winterleitner and David Birlenbach for field assistance, and Winterleitner,David Budd and Peter Eichhubl for discussions that guided our thinking on thisproject. This manuscript benefitted from thoughtful reviews by Haakon Fossen, PeterEichhubl and an anonymous reviewer.

Appendix A

secondary standardization to “absolute reference frame”

The clumped isotope samples in this study were analyzed along with heated gases and carbonatestandards in two analytical sessions (analytical sessions 1 and 2), and we report all of the �47 values both inthe Caltech reference frame and in the “absolute reference frame” described by Dennis and others (2011).The �47 values reported in the Caltech reference frame were normalized to stochastic �47 values andcorrected for linearity and scale compression using CO2 gases heated to 1000 °C (Huntington and others,2009), and the heated gas data used for these normalizations are reported in table A1. The transfer functionfrom the Caltech reference frame to the absolute reference frame was calculated using a secondary


Tab

leA

1

Isot

opic

resu

ltsfo

rhe

ated

gase

s

dat

e δ1

3C

δ1

3C

δ1

8O

gas

δ18

O

δ 47

δ∆

∆∆

∆∆

47

47

47

47

δ 48

48

48

(P

DB

) st

dev

(S

MO

W)

std

ev

(v.

Oz)

st

dev

(v

. O

z)

std

ev

ster

ror

(v.

Oz)

(v

. O

z)

std

ev

Anal

ytic

al S

essi

on 1

, 8/3

1/20

10-9

/11/

2010

: be

st-fi

t hea

ted

gas l

ine:

47

= 0

.010

6 (δ

47) -

0.8

181

(R² =

0.9

7)

9

/1/1

0

-11

.17

0

0.0

03

2

8.7

50

0

.00

8

-4.4

67

0

.01

7

-0.8

85

0

.02

4

0.0

09

8

.81

5

1.4

96

0

.19

1

9/2

/10

-1

0.7

04

0

.00

3

59

.52

2

0.0

09

2

6.7

52

0

.01

4

-0.5

06

0

.03

6

0.0

13

8

6.2

35

1

6.6

86

0

.91

3

9/3

/10

-1

2.3

56

0

.00

3

25

.75

3

0.0

03

-8

.56

3

0.0

22

-0

.87

8

0.0

40

0

.01

4

2.0

81

0

.63

0

0.3

29

9/4

/10

-1

0.6

79

0

.00

3

58

.62

9

0.0

03

2

5.8

55

0

.02

8

-0.5

43

0

.01

7

0.0

06

8

4.4

41

1

6.7

19

0

.87

9

9/5

/10

-1

0.1

91

0

.00

5

58

.12

2

0.0

02

2

5.8

27

0

.01

3

-0.5

57

0

.01

8

0.0

06

8

2.6

74

1

6.0

31

0

.94

6

9/6

/10

-1

0.3

56

0

.00

2

29

.69

6

0.0

03

-2

.69

3

0.0

20

-0

.83

3

0.0

26

0

.00

9

12

.06

4

2.8

74

0

.26

0

9/7

/10

-1

0.7

98

0

.00

4

57

.99

9

0.0

07

2

5.0

88

0

.01

9

-0.5

69

0

.04

0

0.0

14

8

1.5

72

1

5.2

36

2

.23

3

9/8

/10

-1

0.5

88

0

.00

3

29

.31

1

0.0

17

-3

.37

9

0.0

12

-0

.91

4

0.0

73

0

.02

6

10

.89

0

2.4

61

0

.24

5

9/9

/10

-1

0.6

40

0

.00

1

29

.95

0

0.0

02

-2

.74

3

0.0

20

-0

.85

9

0.0

21

0

.00

1

12

.44

5

2.7

57

0

.23

5

9/1

0/1

0

-10

.54

6

0.0

01

2

8.8

41

0

.00

4

-3.7

03

0

.02

0

-0.8

15

0

.02

1

0.0

07

9

.52

6

2.0

21

0

.41

3

9/1

1/1

0

-11

.04

3

0.0

03

2

8.9

79

0

.00

3

-4.0

92

0

.01

3

-0.8

58

0

.03

4

0.0

12

1

0.0

95

2

.32

1

0.3

18

Anal

ytic

al S

essi

on 2

, 8/2

1/20

11-8

/28/

2011

: be

st-fi

t hea

ted

gas l

ine:

47

= 0

.007

5 (δ

47) -

0.7

774

(R² =

0.9

9)

8

/20

/11

-1

0.6

69

0

.00

5

60

.63

1

0.0

05

2

7.8

22

0

.01

4

-0.5

65

0

.03

2

0.0

11

8

3.2

93

1

1.8

16

0

.18

0

8/2

0/1

1

-10

.58

3

0.0

04

2

9.0

47

0

.00

4

-3.5

21

0

.01

8

-0.8

00

0

.02

4

0.0

08

8

.87

8

0.9

79

0

.19

3

8/2

0/1

1

-10

.62

9

0.0

04

6

1.1

20

0

.00

9

28

.35

3

0.0

24

-0

.55

7

0.0

20

0

.00

7

84

.45

9

11

.97

2

0.1

65

8/2

1/1

1

-10

.64

0

0.0

02

2

7.9

28

0

.00

8

-4.6

73

0

.01

8

-0.7

93

0

.01

4

0.0

05

6

.31

1

0.6

04

0

.17

8

8/2

3/1

1

-10

.68

9

0.0

02

5

8.0

61

0

.01

3

25

.23

9

0.0

25

-0

.58

8

0.0

21

0

.00

8

77

.45

1

11

.24

9

0.1

61

8/2

4/1

1

-10

.62

5

0.0

06

2

9.2

47

0

.01

3

-3.3

57

0

.03

0

-0.7

93

0

.03

7

0.0

13

9

.55

1

1.2

56

0

.12

3

8/2

5/1

1

-10

.68

1

0.0

04

5

8.4

38

0

.02

3

25

.62

3

0.0

47

-0

.58

5

0.0

33

0

.01

2

78

.48

5

11

.49

9

0.1

47

8/2

7/1

1

-10

.51

7

0.0

07

2

9.5

32

0

.03

3

-2.9

89

0

.07

3

-0.8

11

0

.03

8

0.0

13

1

0.2

81

1

.42

7

0.2

03

8/2

8/1

1

-10

.65

4

0.0

04

5

7.9

58

0

.01

5

25

.17

4

0.0

62

-0

.58

6

0.0

26

0

.00

9

77

.55

4

11

.54

2

0.1

86

8/2

9/1

1

-10

.39

5

0.0

02

2

9.3

05

0

.00

2

-3.0

91

0

.01

8

-0.8

09

0

.01

8

0.0

06

9

.65

7

1.2

48

0

.23

5

8/3

0/1

1

-10

.60

6

0.0

07

5

8.4

04

0

.01

6

25

.65

9

0.0

25

-0

.58

1

0.0

17

0

.00

6

78

.30

2

11

.37

2

0.1

91

8/3

1/1

1

-10

.65

1

0.0

03

2

9.1

26

0

.00

4

-3.5

12

0

.02

8

-0.7

94

0

.03

2

0.0

11

9

.20

4

1.1

30

0

.16

6

9/1

/11

-1

1.0

07

0

.00

2

56

.92

4

0.0

04

2

3.7

88

0

.03

0

-0.5

89

0

.03

0

0.0

11

7

4.9

60

1

1.0

61

0

.23

8

9/2

/11

-1

0.8

81

0

.00

3

28

.67

6

0.0

04

-4

.19

5

0.0

28

-0

.81

0

0.0

31

0

.01

1

8.2

04

1

.01

2

0.1

94

9/2

/11

-1

0.4

33

0

.00

3

57

.91

7

0.0

13

2

5.3

10

0

.03

3

-0.6

20

0

.03

1

0.0

11

7

7.3

97

1

1.4

52

0

.18

5

9/4

/11

-1

0.7

84

0

.00

4

57

.01

9

0.0

04

2

4.0

94

0

.02

5

-0.6

00

0

.02

5

0.0

09

7

5.3

26

1

1.2

24

0

.22

5

9/6

/11

-1

0.9

84

0

.00

2

28

.19

5

0.0

07

-4

.76

3

0.0

15

-0

.80

4

0.0

29

0

.01

0

7.2

09

0

.96

0

0.1

56

9/7

/11

-1

0.8

79

0

.00

3

56

.04

7

0.0

08

2

3.0

32

0

.01

4

-0.6

06

0

.02

8

0.0

10

7

3.2

04

1

1.0

85

0

.18

6

9/8

/11

-1

0.3

06

0

.00

5

30

.20

2

0.0

03

-2

.13

7

0.0

13

-0

.81

6

0.0

30

0

.01

1

11

.81

6

1.6

24

0

.16

7

9/9

/11

-1

0.4

74

0

.00

3

56

.17

5

0.0

10

2

3.5

70

0

.01

6

-0.5

99

0

.02

3

0.0

08

7

4.1

26

1

1.7

07

0

.14

0

9/1

0/1

1

-10

.61

4

0.0

04

2

9.6

29

0

.00

6

-3.0

00

0

.02

0

-0.8

14

0

.03

8

0.0

14

1

0.6

01

1

.53

6

0.2

81

9/1

1/1

1

-10

.64

1

0.0

03

5

5.7

56

0

.00

5

23

.00

0

0.0

28

-0

.58

8

0.0

29

0

.01

0

72

.87

9

11

.33

6

0.1

90

All

valu

esar

ere

port

edin

‰.“

Oz”

refe

rsto

wor

kin

gre

fere

nce

gas

byO

ztec

h.


Tab

leA

2

Isot

opic

resu

ltsfo

rca

rbon

ate

stan

dard

s

dat

e δ13

C

δ13C

δ1

8O

δ1

8O

δ1

8O

δ 4

7

δ∆

∆

∆

∆∆

47

47

47

∆47

47

∆47

∆

δ 4

8

48

48

HG

st

retc

h

acid

dig

.

(P

DB

) st

dev

C

O2

calc

ite

std

ev

(v.

Oz)

st

dev

(v

. O

z)

std

ev

ster

ror

(v.

Oz)

(v

. O

z)

std

ev

corr

ect.

co

rrec

t.

corr

ect.

(S

MO

W)

(PD

B)

47

Car

rara

Mar

ble,

Ana

lytic

al S

essi

on 1

, 8/3

1/20

10-9

/11/

2010

8/3

0/1

0

2.3

48

0

.00

7

37

.35

6

-1.8

93

0

.03

5

17

.72

2

0.0

27

-0

.40

6

0.0

28

0

.01

0

30

.56

4

6.1

39

0

.84

7

0.2

25

0

.23

2

0.3

12

8/3

1/1

0

2.3

52

0

.00

2

37

.42

1

4.4

71

0

.00

4

17

.81

8

0.0

28

-0

.37

8

0.0

26

0

.00

8

30

.81

3

6.2

57

0

.37

9

0.2

51

0

.25

9

0.3

39

9/1

/10

2

.26

3

0.0

03

3

7.3

44

-1

.90

4

0.0

04

1

7.6

61

0

.01

5

-0.3

72

0

.02

3

0.0

08

3

0.4

35

6

.03

7

0.3

34

0

.25

9

0.2

68

0

.34

8

9/2

/10

2

.32

9

0.0

02

3

7.4

45

-1

.80

7

0.0

03

1

7.8

64

0

.01

7

-0.3

36

0

.04

0

0.0

14

3

1.3

07

6

.69

1

0.4

90

0

.29

3

0.3

03

0

.38

3

9/4

/10

2

.32

2

0.0

03

3

7.3

69

-1

.88

1

0.0

02

1

7.7

38

0

.04

3

-0.3

77

0

.04

4

0.0

08

3

0.8

96

6

.43

9

0.2

05

0

.25

3

0.2

62

0

.34

2

9/5

/10

2

.31

8

0.0

03

3

7.3

27

-1

.92

1

0.0

03

1

7.6

83

0

.01

8

-0.3

86

0

.01

8

0.0

07

3

0.8

98

6

.52

2

0.3

51

0

.24

4

0.2

53

0

.33

3

9/8

/10

2

.34

6

0.0

03

3

7.3

81

-1

.86

9

0.0

05

1

7.8

08

0

.02

2

-0.3

43

0

.04

0

0.0

14

3

1.3

97

6

.90

4

0.2

16

0

.28

6

0.2

96

0

.37

6

9/9

/10

2

.34

6

0.0

03

3

7.4

03

-1

.84

8

0.0

05

1

7.8

16

0

.01

6

-0.3

57

0

.03

4

0.0

12

3

1.4

13

6

.87

8

0.3

72

0

.27

2

0.2

81

0

.36

1

9/1

1/1

0

2.3

39

0

.00

2

37

.40

0

-1.8

50

0

.00

5

17

.80

4

0.0

29

-0

.35

9

0.0

36

0

.01

3

31

.54

2

7.0

09

0

.25

1

0.2

70

0

.27

9

0.3

59

9/1

1/1

0

2.3

43

0

.00

2

37

.47

8

-1.7

75

0

.00

5

17

.87

5

0.0

30

-0

.37

0

0.0

30

0

.01

1

31

.65

1

6.9

64

0

.27

4

0.2

59

0

.26

7

0.3

47

9/1

3/1

0

2.3

08

0

.00

2

37

.40

8

-1.8

43

0

.00

4

17

.75

9

0.0

18

7

-0.3

81

1

0.0

17

1

0.0

06

1

31

.76

4

7.2

10

0

.45

3

0.2

49

0

.25

7

0.3

37

av

era g

e:

0.34

9

stde

v:

0.02

0 C

arm

el C

alci

te, A

naly

tical

Ses

sion

1, 8

/31/

2010

-9/1

1/20

10

8/3

0/1

0

-2.1

08

0

.00

3

35

.14

1

-4.0

24

0

.00

6

11

.39

5

0.0

09

-0

.17

3

0.0

26

0

.00

9

25

.78

4

5.7

79

0

.30

0

0.5

26

0

.54

2

0.6

22

8/3

1/1

0

-2.2

23

0

.00

3

35

.05

6

-4.1

06

0

.00

3

11

.22

5

0.0

19

-0

.14

6

0.0

23

0

.00

8

25

.14

8

5.3

21

0

.31

1

0.5

55

0

.57

2

0.6

52

8/3

1/1

0

-2.1

51

0

.00

2

35

.09

8

-4.0

65

0

.00

3

11

.32

5

0.0

29

-0

.15

8

0.0

30

0

.01

1

25

.07

5

5.1

67

0

.30

4

0.5

41

0

.55

8

0.6

38

9/2

/10

-2

.20

4

0.0

02

3

4.9

64

-4

.19

5

0.0

07

1

1.1

69

0

.02

3

-0.1

29

0

.05

7

0.0

20

2

6.2

33

6

.56

3

1.9

32

0

.57

2

0.5

90

0

.67

0

9/3

/10

-2

.21

7

0.0

03

3

5.0

60

-4

.10

2

0.0

04

1

1.2

58

0

.01

4

-0.1

23

0

.02

9

0.0

10

2

5.1

15

5

.28

1

0.3

42

0

.57

7

0.5

95

0

.67

5

9/3

/10

-1

.16

0

0.0

03

3

0.1

90

-8

.78

8

0.0

03

7

.35

2

0.0

13

-0

.20

6

0.0

34

0

.01

2

13

.53

3

3.3

27

0

.23

7

0.5

35

0

.55

2

0.6

32

9/4

/10

-2

.18

0

0.0

04

3

5.0

78

-4

.08

5

0.0

04

1

1.2

68

0

.02

2

-0.1

67

0

.02

6

0.0

09

2

5.8

41

5

.95

7

0.1

46

0

.53

3

0.5

50

0

.63

0

9/5

/10

-2

.15

3

0.0

04

3

5.0

47

-4

.11

5

0.0

04

1

1.2

79

0

.02

2

-0.1

51

0

.03

7

0.0

13

2

5.4

12

5

.59

6

0.4

40

0

.54

8

0.5

66

0

.64

6

9/7

/10

-2

.19

5

0.0

08

3

4.7

91

-4

.36

1

0.0

12

1

0.9

52

0

.01

7

-0.1

83

0

.02

6

0.0

09

2

4.8

99

5

.58

9

0.3

73

0

.52

1

0.5

37

0

.61

7

9/8

/10

-2

.13

1

0.0

03

3

5.1

05

-4

.05

9

0.0

09

1

1.3

52

0

.01

9

-0.1

57

0

.03

6

0.0

13

2

5.5

99

5

.66

8

0.4

28

0

.54

2

0.5

59

0

.63

9

9/1

0/1

0

-2.1

35

0

.00

4

35

.16

7

-3.9

99

0

.00

4

11

.39

8

0.0

28

-0

.16

9

0.0

45

0

.01

6

25

.95

6

5.8

97

0

.25

3

0.5

30

0

.54

6

0.6

26

9/1

2/1

0

-2.1

43

0

.00

3

35

.18

7

-3.9

80

0

.00

3

11

.44

7

0.0

22

-0

.13

3

0.0

29

0

.01

0

25

.94

4

5.8

46

0

.43

9

0.5

65

0

.58

3

0.6

63

av

era g

e:

0.64

3

stde

v:

0.01

9


Tab

leA

2

(con

tinue

d)

dat

e δ13

C

δ13C

δ1

8O

δ1

8O

δ1

8O

δ 4

7

δ∆

47

47

∆

∆

∆∆

47

∆∆

47

47

∆47

δ 48

48

48

HG

st

retc

h

acid

dig

.

(P

DB

) st

dev

C

O2

calc

ite

std

ev

(v.

Oz)

st

dev

(v

. O

z)

std

ev

ster

ror

(v.

Oz)

(v

. O

z)

std

ev

corr

ect.

co

rrec

t.

corr

ect.

(S

MO

W)

(PD

B)

47

Car

rara

Mar

ble,

Ana

lytic

al S

essi

on 2

, 8/2

1/20

11-8

/28/

2011

8/2

0/1

1

2.3

54

0

.00

3

37

.31

6

-1.9

31

0

.00

6

17

.69

2

0.0

25

-0

.40

2

0.0

30

0

.01

1

28

.23

5

3.9

43

0

.21

3

0.2

43

0

.26

4

0.3

44

8/2

1/1

1

2.3

52

0

.00

3

37

.33

4

-1.9

14

0

.00

5

17

.71

7

0.0

19

-0

.39

2

0.0

26

0

.00

9

28

.43

0

4.0

98

0

.18

6

0.2

53

0

.27

5

0.3

55

8/2

2/1

1

2.3

54

0

.00

3

37

.34

6

-1.9

03

0

.00

6

17

.73

8

0.0

25

-0

.38

5

0.0

14

0

.00

5

28

.38

3

4.0

30

0

.12

9

0.2

60

0

.28

2

0.3

62

8/2

5/1

1

2.3

57

0

.00

3

37

.34

0

-1.9

08

0

.01

2

17

.74

1

0.0

22

-0

.37

9

0.0

30

0

.01

1

28

.54

8

4.2

02

0

.18

4

0.2

65

0

.28

9

0.3

69

8/2

6/1

1

2.3

53

0

.00

5

37

.32

5

-1.9

23

0

.02

6

17

.72

4

0.0

27

-0

.37

8

0.0

28

0

.01

0

28

.65

5

4.3

36

0

.19

1

0.2

66

0

.29

0

0.3

70

8/2

8/1

1

2.3

60

0

.00

6

37

.40

4

-1.8

47

0

.03

4

17

.80

4

0.0

61

-0

.38

3

0.0

33

0

.01

2

28

.83

0

4.3

55

0

.17

4

0.2

61

0

.28

4

0.3

64

8/2

9/1

1

2.3

75

0

.00

2

37

.38

0

-1.8

70

0

.00

9

17

.78

7

0.0

22

-0

.38

1

0.0

22

0

.00

8

28

.63

7

4.1

92

0

.15

4

0.2

63

0

.28

6

0.3

66

8/2

9/1

1

2.3

80

0

.00

4

37

.32

1

-1.9

27

0

.00

4

17

.71

9

0.0

23

-0

.39

4

0.0

26

0

.00

9

28

.51

2

4.1

85

0

.10

1

0.2

51

0

.27

2

0.3

52

8/3

0/1

1

2.3

21

0

.00

2

37

.40

7

-1.8

44

0

.00

6

17

.73

8

0.0

26

-0

.40

4

0.0

27

0

.00

9

28

.87

8

4.3

76

0

.12

2

0.2

40

0

.26

1

0.3

41

9/1

/11

2

.22

8

0.0

03

3

7.2

60

-1

.98

6

0.0

04

1

7.4

96

0

.03

1

-0.4

08

0

.02

6

0.0

09

2

8.6

35

4

.42

4

0.1

99

0

.23

8

0.2

59

0

.33

9

9/3

/11

2

.35

9

0.0

04

3

7.3

42

-1

.90

6

0.0

03

1

7.7

29

0

.02

4

-0.3

85

0

.01

8

0.0

06

2

8.8

84

4

.50

6

0.1

39

0

.25

9

0.2

82

0

.36

2

9/4

/11

2

.35

7

0.0

02

3

7.3

71

-1

.87

9

0.0

04

1

7.7

50

0

.03

6

-0.3

92

0

.03

4

0.0

12

2

8.9

07

4

.47

4

0.0

79

0

.25

3

0.2

75

0

.35

5

9/6

/11

2

.37

8

0.0

03

3

7.3

51

-1

.89

8

0.0

04

1

7.7

52

0

.00

9

-0.3

90

0

.01

9

0.0

07

2

8.7

59

4

.36

8

0.0

71

0

.25

4

0.2

77

0

.35

7

9/7

/11

2

.38

1

0.0

04

3

7.3

55

-1

.89

4

0.0

10

1

7.7

60

0

.01

7

-0.3

89

0

.01

1

0.0

04

2

8.9

28

4

.52

5

0.1

72

0

.25

5

0.2

77

0

.35

7

9/8

/11

2

.38

2

0.0

04

3

7.3

18

-1

.92

9

0.0

06

1

7.6

86

0

.02

2

-0.4

27

0

.01

9

0.0

07

2

8.7

03

4

.37

6

0.1

05

0

.21

8

0.2

37

0

.31

7

9/9

/11

2

.38

2

0.0

03

3

7.2

64

-1

.98

2

0.0

03

1

7.6

38

0

.02

8

-0.4

21

0

.02

5

0.0

09

2

8.8

01

4

.57

7

0.1

76

0

.22

4

0.2

44

0

.32

4

9/1

0/1

1

2.3

80

0

.00

4

37

.33

5

-1.9

13

0

.00

3

17

.73

8

0.0

11

-0

.39

0

0.0

23

0

.00

8

28

.98

8

4.6

23

0

.12

5

0.2

55

0

.27

7

0.3

57

9/1

0/1

1

2.3

76

0

.00

3

37

.31

3

-1.9

35

0

.00

4

17

.71

5

0.0

21

-0

.38

7

0.0

30

0

.01

1

28

.84

0

4.5

21

0

.15

0

0.2

58

0

.28

0

0.3

60

9/1

1/1

1

2.3

80

0

.00

2

37

.38

4

-1.8

66

0

.00

4

17

.84

5

0.0

19

-0

.33

4

0.0

24

0

.00

9

29

.18

8

4.7

23

0

.16

4

0.3

10

0

.33

7

0.4

17

9/1

2/1

1

2.3

84

0

.00

3

37

.37

4

-1.8

76

0

.00

3

17

.76

5

0.0

09

-0

.40

6

0.0

27

0

.00

9

29

.20

6

4.7

60

0

.15

1

0.2

39

0

.25

9

0.3

39

av

era g

e:

0.3

55

st

dev

: 0

.02

0

TV-0

1 C

alci

te, A

naly

tical

Ses

sion

2, 8

/21/

2011

-8/2

8/20

11:

8/2

1/1

1

2.3

95

0

.00

3

30

.49

4

-8.4

96

0

.00

7

11

.15

6

0.0

20

-0

.15

8

0.0

29

0

.01

0

12

.54

7

1.7

46

0

.13

3

0.5

35

0

.58

2

0.6

62

8/2

1/1

1

2.4

94

0

.00

2

30

.49

3

-8.4

96

0

.00

7

11

.26

7

0.0

17

-0

.14

4

0.0

28

0

.01

0

12

.64

9

1.8

47

0

.22

7

0.5

49

0

.59

7

0.6

77

8/2

2/1

1

2.5

90

0

.00

4

30

.43

9

-8.5

49

0

.00

8

11

.32

3

0.0

15

-0

.12

7

0.0

28

0

.01

0

12

.25

6

1.5

63

0

.12

9

0.5

66

0

.61

5

0.6

95

8/2

3/1

1

2.5

96

0

.00

4

30

.43

6

-8.5

51

0

.02

1

11

.28

7

0.1

12

-0

.16

6

0.0

27

0

.00

9

12

.46

4

1.7

73

0

.16

2

0.5

27

0

.57

3

0.6

53

8/2

6/1

1

2.5

45

0

.00

3

30

.41

7

-8.5

69

0

.00

7

11

.22

7

0.0

21

-0

.15

8

0.0

16

0

.00

6

12

.57

8

1.9

23

0

.18

5

0.5

35

0

.58

2

0.6

62

8/2

7/1

1

2.6

22

0

.00

5

30

.38

2

-8.6

03

0

.01

2

11

.25

5

0.0

22

-0

.16

9

0.0

14

0

.00

5

12

.47

2

1.8

88

0

.18

1

0.5

24

0

.57

0

0.6

50

8/2

9/1

1

2.6

56

0

.00

3

30

.41

8

-8.5

69

0

.00

4

11

.30

8

0.0

10

-0

.17

5

0.0

12

0

.00

4

12

.71

7

2.0

40

0

.12

0

0.5

17

0

.56

2

0.6

42

8/2

9/1

1

2.6

60

0

.00

2

30

.44

4

-8.5

43

0

.00

7

11

.34

2

0.0

24

-0

.17

2

0.0

23

0

.00

8

12

.60

6

1.8

79

0

.25

2

0.5

20

0

.56

6

0.6

46


Tab

leA

2

(con

tinue

d)

dat

e δ13

C

δ13C

δ1

8O

δ1

8O

δ1

8O

δ 4

7

δ∆

47

47

∆

47

∆47

∆

∆∆

47

δ 48

48

48

HG

st

retc

h

acid

dig

.

(P

DB

) st

dev

C

O2

calc

ite

std

ev

(v.

Oz)

st

dev

(v

. O

z)

std

ev

ster

ror

(v.

Oz)

(v

. O

z)

std

ev

corr

ect.

co

rrec

t.

corr

ect.

(S

MO

W)

(PD

B)

∆

∆47

47

TV-0

1 C

alci

te, A

naly

tical

Ses

sion

2, 8

/21/

2011

-8/2

8/20

11:

8/3

1/1

1

2.3

93

0

.00

2

30

.68

9

-8.3

08

0

.00

4

11

.34

1

0.0

26

-0

.15

9

0.0

28

0

.01

0

13

.30

7

2.0

98

0

.09

5

0.5

34

0

.58

0

0.6

60

9/2

/11

2

.64

6

0.0

02

3

0.4

40

-8

.54

7

0.0

04

1

1.3

35

0

.02

7

-0.1

61

0

.02

6

0.0

09

1

2.8

01

2

.08

0

0.2

44

0

.53

2

0.5

78

0

.65

8

9/6

/11

2

.60

3

0.0

03

3

0.4

92

-8

.49

7

0.0

07

1

1.3

49

0

.02

2

-0.1

58

0

.03

6

0.0

13

1

2.8

74

2

.05

2

0.2

34

0

.53

5

0.5

81

0

.66

1

9/8

/11

2

.54

3

0.0

04

3

0.3

87

-8

.59

8

0.0

06

1

1.1

59

0

.02

0

-0.1

83

0

.02

1

0.0

08

1

2.4

50

1

.83

7

0.1

57

0

.51

0

0.5

55

0

.63

5

9/8

/11

2

.59

3

0.0

04

3

0.3

70

-8

.61

4

0.0

04

1

1.1

85

0

.01

2

-0.1

89

0

.02

8

0.0

10

1

2.4

64

1

.88

3

0.1

55

0

.50

5

0.5

49

0

.62

9

9/8

/11

2

.61

8

0.0

04

3

0.4

77

-8

.51

1

0.0

08

1

1.3

03

0

.02

0

-0.2

03

0

.02

1

0.0

07

1

2.6

82

1

.89

0

0.1

92

0

.49

0

0.5

33

0

.61

3

9/1

0/1

1

2.5

62

0

.00

5

30

.42

2

-8.5

64

0

.00

3

11

.22

7

0.0

21

-0

.16

9

0.0

27

0

.00

9

12

.83

1

2.1

45

0

.16

3

0.5

24

0

.57

0

0.6

50

9/1

0/1

1

2.5

75

0

.00

3

30

.40

7

-8.5

79

0

.00

3

11

.22

5

0.0

22

-0

.16

9

0.0

28

0

.01

0

12

.76

4

2.1

09

0

.18

4

0.5

25

0

.57

1

0.6

51

9/1

2/1

1

2.5

70

0

.00

3

30

.40

1

-8.5

85

0

.00

5

11

.21

2

0.0

14

-0

.17

1

0.0

41

0

.01

5

12

.73

7

2.0

92

0

.11

8

0.5

22

0

.56

7

0.6

47

av

erag

e:

0.6

52

st

dev

: 0

.01

8

NBS

-19

Cal

cite

, Ana

l ytic

al S

essi

on 2

, 8/2

1/20

11-8

/28/

2011

:

8

/24

/11

2

.05

3

0.0

04

3

6.9

63

-2

.27

2

0.0

16

1

7.0

75

0

.02

9

-0.3

71

0

.03

7

0.0

13

2

7.6

70

4

.07

6

0.1

39

0

.27

8

0.3

03

0

.38

3

8/2

7/1

1

2.0

47

0

.00

4

36

.94

2

-2.2

92

0

.00

8

17

.03

5

0.0

26

-0

.38

4

0.0

22

0

.00

8

27

.75

0

4.1

95

0

.23

7

0.2

66

0

.28

9

0.3

69

8/2

8/1

1

2.0

55

0

.00

4

36

.97

4

-2.2

61

0

.01

4

17

.08

0

0.0

25

-0

.37

9

0.0

27

0

.01

0

27

.85

4

4.2

35

0

.12

3

0.2

71

0

.29

4

0.3

74

av

erag

e:

0.3

75

st

dev

: 0

.00

7

All

valu

esar

ere

port

edin

‰.“

Oz”

refe

rsto

wor

kin

gre

fere

nce

gas

byO

ztec

h.


standardization, which uses assumed �47 values for these 1000 °C heated gases and measured and assumed�47 values for carbonate standards. Table A2 presents the isotopic results for the carbonate standards(Carrara marble, TV-01 calcite, and Carmel calcite). Table A3 summarizes the information derived from thedata in tables A1 and A2, along with the accepted �47 values for these samples in the absolute referenceframe. The transfer function from the Caltech reference frame to the absolute reference frame did notchange between analytical sessions 1 and 2, so a single transfer function is reported in table A3 and used toreference the results presented in table 1.

References

Anderson, M. P., 2005, Heat as a ground water tracer: Groundwater, v. 43, n. 6, p. 951–968, http://dx.doi.org/10.1111/j.1745-6584.2005.00052.x

Antonellini, M., and Aydin, A., 1994, Effect of faulting on fluid flow in porous sandstones: petrophysicalproperties: AAPG Bulletin, v. 78, n. 3, p. 355–377.

Aydin, A., 2000, Fractures, faults, and hydrocarbon entrapment, migration and flow: Marine and PetroleumGeology, v. 17, n. 7, p. 797–814, http://dx.doi.org/10.1016/S0264-8172(00)00020-9

Aydin, A., and Johnson, A. M., 1978, Development of faults as zones of deformation bands and as slip surfacesin sandstone: Pure and Applied Geophysics, v. 116, n. 4–5, p. 931–942, http://dx.doi.org/10.1007/BF00876547

Boggs, S., and Krinsley, D., 2006, Application of cathodoluminescence imaging to the study of sedimentaryrocks: Cambridge, Cambridge University Press, 165 p.

Boles, J. R., Eichhubl, P., Garven, G., and Chen, J., 2004, Evolution of a hydrocarbon migration pathwayalong basin-bounding faults: Evidence from fault cement: AAPG Bulletin, v. 88, p. 947–970, http://dx.doi.org/10.1306/02090403040

Caine, J. S., Evans, J. P., and Forster, C. B., 1996, Fault zone architecture and permeability structure: Geology,v. 24, n. 11, p. 1025–1028, http://dx.doi.org/10.1130/0091-7613(1996)024 1025:FZAAPS�2.3.CO;2

Chan, M. A., Parry, W. T., and Bowman, J. R., 2000, Diagenetic hematite and manganese oxides andfault-related fluid flow in Jurassic sandstones, southeastern Utah: AAPG Bulletin, v. 84, n. 9, p. 1281–1310, http://dx.doi.org/10.1306/A9673E82-1738-11D7-8645000102C1865D

Davatzes, N., and Aydin, A., 2003, Overprinting faulting mechanisms in high porosity sandstones of SE Utah:Journal of Structural Geology, v. 25, n. 11, p. 1795–1813, http://dx.doi.org/10.1016/S0191-8141(03)00043-9

Davatzes, N. C., Aydin, A., and Eichhubl, P., 2003, Overprinting faulting mechanisms during the develop-ment of multiple fault sets in sandstone, Chimney Rock fault array, Utah, USA: Tectonophysics, v. 363,n. 1–2, p. 1–18, http://dx.doi.org/10.1016/S0040-1951(02)00647-9

Davatzes, N. C., Eichhubl, P., and Aydin, A., 2005, Structural evolution of fault zones in sandstone bymultiple deformation mechanisms: Moab fault, southeast Utah: Geological Society of America Bulletin,v. 117, n. 1–2, p. 135–148, http://dx.doi.org/10.1130/B25473.1

Dennis, K. J., and Schrag, D. P., 2010, Clumped isotope thermometry of carbonatites as an indicator ofdiagenetic alteration: Geochimica et Cosmochimica Acta, v. 74, n. 15, p. 4110–4122, http://dx.doi.org/10.1016/j.gca.2010.04.005

Dennis, K. J., Affek, H. P., Passey, B. H., Schrag, D. P., and Eiler, J. M., 2011. Defining an absolute referenceframe for “clumped” isotope studies of CO2: Geochimica et Cosmochimica Acta, v. 75, n. 22, p. 7117–7131, http://dx.doi.org/10.1016/j.gca.2011.09.025

Doelling, H., 1985, Geologic map of Arches National Park and vicinity, Grand County, Utah: Salt Lake City,Utah, Utah Geological and Mineral Survey, Map 74, scale 1:50,000.

–––––– 2002, Geologic map of the Moab 7.5� quadrangle, Grand County, Utah: Salt Lake City, Utah, UtahGeological Survey, Utah Department of Natural Resources.

Eichhubl, P., Greene, H. G., Naehr, T., and Maher, N., 2000, Structural control of fluid flow: offshore fluid

Table A3

Summary of transfer function data for the absolute reference frame

sample analytical session source of accepted value

HG Sessions 1 & 2 0.000 0.0266 Dennis and others, 2011

Carrara Session 1 0.349 0.395 Dennis and others, 2011

Carmel Session 1 0.643 0.705 H. Affek, pers. comm. 2012

Carrara Session 2 0.355 0.395 Dennis and others, 2011

TV-01 Session 2 0.652 0.713 J. Eiler, pers. comm. 2012

NBS-19 Session 2 0.375 0.392 Dennis and others, 2011

accepted ∆ 47 (‰) measured ∆ 47 (‰)

Transfer function from Caltech reference frame to absolute reference frame: �47, ARF � 1.0567 (�47,Caltech) � 0.0197 (R2 � 0.99777).


seepage in the Santa Barbara Basin, California: Journal of Geochemical Exploration, v. 69–70, p. 545–549, http://dx.doi.org/10.1016/S0375-6742(00)00107-2

Eichhubl, P., Taylor, W. L., Pollard, D. D., and Aydin, A., 2004: Paleo-fluid flow and deformation in the Aztecsandstone at the Valley of Fire, Nevada—evidence for the coupling of hydrogeologic, diagenetic, andtectonic processes: Geological Society of America Bulletin, v. 116, n. 9–10, p. 1120–1136, http://dx.doi.org/10.1130/B25446.1

Eichhubl, P., Davatz, N. C., and Becker, S. P., 2009, Structural and diagenetic control of fluid migration andcementation along the Moab fault, Utah: AAPG Bulletin, v. 93, n. 5, p. 653–681, http://dx.doi.org/10.1306/02180908080

Eiler, J. M., 2007, “Clumped-isotope” geochemistry—The study of naturally-occurring, multiply-substitutedisotopologues: Earth and Planetary Science Letters, v. 262, n. 3–4, p. 309–327, http://dx.doi.org/10.1016/j.epsl.2007.08.020

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