Periglacial Process and Landforms ESCI 307 Fall 2003 Lecture 18 Periglacial Process and Landforms

Permafrost distribution in the Arctic high latitudes

Periglacial (tundra) environments ESCI 307 Fall 2003 Lecture 18 Periglacial (tundra) environments Alpine tundra Arctic tundra

Permafrost Perennially frozen ground that remains at or below 0 C (32 F) for two or more years Forms in regions where the mean annual temperature is colder than 0 C Permafrost underlies about 20% of the land in the Northern Hemisphere also common within the Arctic Ocean’s continental shelves and in parts of Antarctica Most of the world’s permafrost has been frozen for millennia and can be up to 5,000 ft thick.

Active Layer vs Permafrost: Thermal State “Active layer”: “thermal boundary layer”; near surface, seasonally thawed Depth at which annual max temp = 0C Water content, soil strength, and bulk density of soil change dramatically Produces patterned ground/solifluction Drives hydrology of periglacial landscapes Perenially frozen ground: permafrost Material at < 0C for 2 yrs or more Sub-freezing thermal state

Temperature Profile Base of active layer = depth where Tmax = 0C Below active layer, mean annual temp increases (geothermal gradient) to 0C This is the base of permafrost Thickness of permafrost most strongly controlled by mean annual surface temp As mean annual surface temp decreases, permafrost deepens, active layer thins

What sets the depth of the active layer? annual temp swings (Tamp) falls off exponentially with depth at a depth of z*, the amplitude or temp swing is 1/3 of that at the surface Mean annual surface temp Oscillation of temp about the mean Oscillations decrease with depth Time lag of oscillations geothermal heat flow Temp (depth, time) Thermal behavior Of Periglacial Landscapes depth scale = f(thermal diffusivity, period) ~ 3m.

Ground temperatures Mean T increases with depth Permafrost Seasonal ESCI 307 Fall 2003 Lecture 18 Ground temperatures Mean T increases with depth Permafrost Active layer to Base of p’frost Seasonal Geomorphic work Active layer Above ZAA 25C/km = .025C/m

Depth of the active layer Solve for depth Z*=depth scale P=period of oscillation, 1 yr k=thermal diffusivity of regolith, 1mm2/s Z* ~ 3m If Tamp < mean surface temp, active layer depth = 0 That means it’s frozen all the time, all permafrost

Below the active layer… Single borehole at E. Teshekpuk Lake, AK 70 degrees latitude Clow, 2008 There is no liquid water so heat moves by conduction, Q=-k(dT/dz) Why do model and data vary near surface? Variation in k with depth? Msmts say no Long-term Arctic warming Lachenbruch and Marshall, 1986

Types of Ice Pore Segregation Massive ground ice Frozen in interstitial space between particles Segregation Lenses of ice in fine grained sediment, commonly parallel to ground surface Ice content can exceed porosity Massive ground ice

Frost Heave Water migrates through fine grained (silty) material to lenses of ice (segregation ice) Even against gravity (capillary action) Ice lenses redistribute moisture As lenses grow, they deform soil and lift ground surface Frost heave Slower rates of freezing allow for more time for water migration Amount of heave = f(water content, soil texture, rate of freezing)

Upfreezing of stones Frost heave is the process that enables upward transport of stones to the ground surface Upfreezing or frost-jacking Sorting occurs due to long-term effects of upfreezing on unsorted mixed grain size sediments

Frost pull Requires frost susceptible soil with scattered large stones Clast moves up with frost heaving soil Clast adhered to froz soil Void beneath clast fills upon thaw Requires frost susceptible soil with scattered large stones

Patterned ground Geometric or repeated patterns on the ground surface Sorting, variations in vegetation, microtopography Seasonal heaving of the active layer and radial surface motion Controlled by depth of active layer Sorted circles: self organized

Yipes – stripes! ESCI 307 Fall 2003 Lecture 18

Boxes A and B: Lateral sorting Boxes A, C, and D: Lateral squeezing and confinement Stones creep to stones Soil moves toward deeper soil Vertical frost heave Lateral frost heave Areas of concentrated stones uplift by lateral sqeezing Stones avalanche off sides and move along stone axis Kessler and Lerner, 2003

Self organization “nonlinear, dissipative interactions among the small- and fastscale constituents of a system give rise to order at larger spatial and longer temporal scales” (Kessler and Lerner, 2003)

Ice Wedge Polygons Tapering vertical wedges of ice Grow by repeated thermal contraction cracking of frozen ground Ice growth in the cracks from summer meltwater

Thermal contraction produces horiz. tensile stress Tensile stress > tensile strength of froz ground: Crack Crack propagates downward Fills with snow, water, and freezes

Fossil Frost Wedges Big Horn Basin Pipeline trench ESCI 307 Fall 2003 Lecture 18 Fossil Frost Wedges Cover sand (eolian)? Big Horn Basin Pipeline trench Bkb (caliche) Preglacial soil

Polygon Geometry A crack relieves stresses that led to its formation (normal to the crack) Remaining stress is || to the crack New cracks intersect perpendicular to crack “cracks nucleate in random directions, but intersect one another at right angles” Random orthogonal networks Scale of cracks related to depth of crack

Alpine Felsenmeer (CO Front Range) Making Felsenmeer (out of ice cubes and a Hershey bar) http://www.sciencefriday.com/videos/watch/10299

Solifluction Lobate features produced by slow creep assoc. with frost action Fronted by rocks or rolls of tundra vegetation Can occur in “sheets” on low gradient slopes Often in hillslope hollows/concavities where flowlines converge Higher moisture content than surrounding ground, denser vegetation http://pyrn.ways.org/cryoplanation-terrace

Soli-/Gelifluction ESCI 307 Fall 2003 Lecture 18

Planview map of solifluction lobe, NE Greenland

Examples: soli-fluction ESCI 307 Fall 2003 Lecture 18 Examples: soli-fluction Cryoplanation? production of an erosional surface by freeze-thaw and other periglacial processes step- or table like residual landforms consisting of a nearly horizontal bedrock surface covered by a thin veneer of rock debris, produced by frost action

Stone lobes ESCI 307 Fall 2003 Lecture 18

Block streams ESCI 307 Fall 2003 Lecture 18

Pingos Conical mound Cored by massive ice Height: 1-10 m., Dia.: 50-150 m. Require permafrost Often found on the bed of drained lakes Closed system pingo Water derived from talik (localized unfrozen ground) Open system pingo Water derived from groundwater

How to make a pingo Step 1: Lake drains ESCI 307 Fall 2003 Lecture 18 Step 1: Lake drains Step 2: Ice segregation by pore water movement into talik Step 3: Ice grows from top; fed by talik water

“Hydrolaccoliths”

Periglacial Landforms in Google Earth Arctic coastal plain, Point Barrow, AK Kings Hill, ID Northwest Territories, Canada