1. Quantifying Desert Surface Processes Using 10 Be and 26 Al Kyle K. Nichols School of Natural Resources

2. What is a desert piedmont?

3. Three common types of desert piedmonts Erosional Depositional

4. Why should we care about piedmonts? Ubiquitous landforms in the American southwest (and in all deserts worldwide) Easily developed (low gradient, sediment cover easy to excavate) Greatly studied (100+ years), but long- term process rates are poorly quantified (slow rates of change)

5. Quantify long-term process rates to understand the background dynamics of piedmonts Quantify short-term processes to determine present day behavior piedmonts Compare the rates to understand human impact on desert ecosystem Need to understand long-term piedmont processes (and short-term too!)

6. Yucca Mountain

10. Chemehuevi Mountain

11. East Range Road

12. Cosmogenic Nuclides Si O Ca, K, Cl 26 Al, 21 Ne, 3 He 10 Be, 14 C, 3 He 36 Cl, 3 He The isotopes are like a suntan.

13. Why use 10 Be and 26 Al? Target mineral is quartz, an abundant mineral on Earth Production rates are well known (Nishiizumi et al., 1989; Clark et al., 1995; Bierman et al., 1996; Larsen et al., in revision) Latitude and altitude corrections are well known (Lal, 1991; Dunai, 2000) Use as dosimeters to model near surface history

14. 10 Be and 26 Al for desert piedmonts Measure 10 Be and 26 Al in sediment to quantify –sediment yield from source basins at top of piedmont –Sediment transport across piedmonts –Long-term surface histories (such as deposition) on piedmont (if any)

15. Depth profile of 10 Be production in sediment

17. CP1 CP2

26. Field Methods Three types of samples –Source basin sample –Transect samples –Soil pit samples Provides a 4-D look into piedmont processes

27. Source basin samples

28. Transect Samples Ephemeral Channels Incised alluvium Bedrock Colluvium

29. Logistical nightmare

30. Soil pit samples

31. Soil pit sampling

32. Shallow Soil Pits Active Transport Layer

33. Laboratory Methods Sieve sediment for 0.5 to 0.85 mm Separate quartz with HCl and HF/Nitric acid baths Dissolve quartz and extract Be and Al Analyze for ratios ( 10 Be: 9 Be and 26 Al: 27 Al) at LLNL on AMS

34. Chemehuevi Transect Samples Ephemeral channel sediment

35. Chemehuevi Transect Samples Incised alluvial sediment

36. Chemehuevi Transect Samples Bedrock and colluvium sediment

37. Chemehuevi Transect Samples Sawtooth Range sediment

39. Sediment from uplands Depth (cm) 10 Be activity (atoms g -1 ) Active layer Fixed location - constant 10 Be inventory Deposition signature

40. Sediment Depth (cm) 10 Be activity (atoms g -1 )

41. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 )

42. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 )

43. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 )

44. Hiatus in deposition Sediment Depth (cm) 10 Be activity (atoms g -1 )

45. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 )

46. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 ) Higher 10 Be activity

47. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 ) Higher 10 Be activity

48. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 ) Higher 10 Be activity

49. Deposition signature Sediment Depth (cm) 10 Be activity (atoms g -1 ) Higher 10 Be activity

50. CP2 - wash surface 12 km from mountain front

51. 18 mm ky -1 37 mm ky -1

52. Rapid deposition followed by stable surface Depth (cm) 10 Be activity (atoms g -1 )

53. Rapid deposition followed by stable surface Depth (cm) 10 Be activity (atoms g -1 )

54. CP1 - proximal surface 6 km from mountain front

55. CP1 18 mm ky -1

56. Soil Pit comparison Deposition 18 mm ky -1 from 70 to ~34 ky ago piedmont wide (both soil pits) Erosion of alluvial sediment ~34 ky ago (CP1) Increased deposition rates (37 mm ky -1 ) on wash surface and higher nuclide activities ~34 ky ago (CP2) Change from sediment deposition to transport on wash surface ~ 8 ky ago

57. Model Equation Sediment in Sediment out Sediment deposition Sediment erosion

58. Chemehuevi Ephemeral Channel Samples

59. Sediment velocities 8 cm y -1 39 cm y -1

60. Iron and Granite Mountain piedmonts

61. Chemehuevi vs. Iron and Granite

64. Iron and Granite Mountain piedmonts Simple surface (no incision, channels migrate similar to distal Chemehuevi Mountain piedmont)

65. Iron and Granite Mountain piedmonts Simple surface (no incision, channels migrate similar to distal Chemehuevi Mountain piedmont) Deposition rates 17 to 37 mm ky -1 (same as Chemehuevi Mountain piedmont)

66. Iron and Granite Mountain piedmonts Simple surface (no incision, channels migrate similar to distal Chemehuevi Mountain piedmont) Deposition rates 17 to 37 mm ky -1 (same as Chemehuevi Mountain piedmont) Depositional hiatus at Holocene-Pleistocene climate transition (~10 ky ago)

67. Iron and Granite Mountain piedmonts Simple surface (no incision, channels migrate similar to distal Chemehuevi Mountain piedmont) Deposition rates 17 to 37 mm ky -1 (same as Chemehuevi Mountain piedmont) Depositional hiatus at Holocene-Pleistocene climate transition (~10 ky ago) Sediment velocities are decimeters per year

68. Conclusions Sediment velocities are not dependent on piedmont morphology (simple vs. complex)

70. East Range Road Upper Surface

71. East Range Road Wash Surface

72. Source Basin Sample

73. Three common types of desert piedmonts Erosional Depositional

74. East Range Road

76. Transect data

77. Rapid deposition followed by stable surface Depth (cm) 10 Be activity (atoms g -1 )

78. Rapid deposition followed by stable surface Depth (cm) 10 Be activity (atoms g -1 )

79. 76 ky EP1

80. EP2 No nuclide dependence with depth!

82. 7 to 10 ky 15 to 25 ky 20 ky 40 – 150 mm ky -1 80 – 100 mm ky -1

84. Conclusions Sediment velocities are not dependent on piedmont morphology (simple vs. complex) Sediment velocities are the same for undisturbed and disturbed piedmonts

85. Conclusions Sediment velocities are not dependent on piedmont morphology (simple vs. complex) Sediment velocities are the same for undisturbed and disturbed piedmonts Large-scale structural controls do not affect long term process rates

86. Conclusions Sediment velocities are not dependent on piedmont morphology (simple vs. complex) Sediment velocities are the same for undisturbed and disturbed piedmonts Large-scale structural controls do not affect long term process rates Quantify baseline process rates on disturbed piedmonts

87. What effect do Army tanks have on sediment movement?

88. Pebbles

89. Long-term vs. Short-term Long-term sediment movement based on cosmogenic nuclides is 8 to 23 cm y -1

90. Long-term vs. Short-term Long-term sediment movement based on cosmogenic nuclides is 8 to 23 cm y -1 Contemporary measurements suggest sediment movement is 80 cm y -1

91. Long-term vs. Short-term Long-term sediment movement based on cosmogenic nuclides is 8 to 23 cm y -1 Contemporary measurements suggest sediment movement is 80 cm y -1 Disturbance by tanks, trucks, and troops increases sediment movement from 4 to 10 fold!

92. Conclusions Sediment velocities are not dependent on piedmont morphology (simple vs. complex) Sediment velocities are the same for undisturbed and disturbed piedmonts Quantify baseline process rates on disturbed piedmonts Large-scale structural controls do not affect long term process rates Contemporary sediment movement rates can be up to 10 fold greater than baseline rates on disturbed piedmonts

93. Acknowledgements Funding from DEPSCoR grant #DAAD199910143 and the Jonathan O. Davis and J. Hoover Mackin scholarships Ruth Sparks and the ITAM crew at Ft. Irwin for logistical support Needles BLM crew for Chemehuevi soil pits Missy Eppes for soils descriptions

95. Thanks Lyman!

96. Thanks Paul !