Management of Subterranean Ecosystems in Extreme Environments
Eastern Nevada caving
Cave Development in Eastern Nevada
A Broad-brush Synopsis
Eastern Nevada Caving

Photo by Dave Bunnell, UnderEarth Graphics

Most of the caves of eastern Nevada have formed in beds of relatively pure to somewhat cherty limestone. During the Paleozoic Era, roughly between 542 and 251 million years ago, most of the sedimentary rocks present in Nevada south of a diagonal line drawn from Lake Tahoe on the California-Nevada border and the extreme northeastern tip of the state were deposited in shallow seas west of the nascent North America continent. Subsequently, continental scale crustal movements carried North America west and bumped into these shallow water rocks, plastering them against the continental borderlands. The oceans came and went as the North American tectonic plate slowly pushed its way westward, burying these rocks, twisting them and squeezing them into limestone, some with thin stringers of chert. Most of this rock torture took place in the following Mesozoic Era that stretched between about 245 and 65 million years ago. Some of these older rocks were pushed deep into the crust where they melted and gradually rose to form large masses or plutons of granitic rock. These plutons are largely responsible for the extensive and varied ore deposits such as the Comstock Lode (the richest single ore deposit ever found) that Nevada is famous for. Concurrently, other slabs of rock to the east were intruded with granitic rock and buckled up to form the Rocky Mountains at what was then the western edge of North America.

At about the end of the Mesozoic at the climax of the Age of Dinosaurs some 65 million years ago, a large slab of the adjacent old Pacific Ocean bottom to the west was over-ridden and supposedly sank into the Earth's crust to be consumed and recycled as granitic rocks as already mentioned. This slab of California rock, however, as was typical of most things Californian, was a non-conformist and instead pushed its way east under the western edge of North America to about where Salt Lake City stands today. The resulting upward bowing of the crust stretched it apart. Formerly quiet slabs of rock were fractured to start forming the Great Basin. Gradually the entire area started to settle down a bit, but because of continued continental unrest, these rocks were faulted up with their western edges higher than the foundering eastern edges to form the north-southtrending mountain ranges of the Great Basin that geographers have likened to an army of caterpillars slowly inching their way north from Mexico. To the northwest, long offshore volcanic island chains belched forth large amounts of lava, volcanic ash, and allied sediments that even had a few offshore coral reefs that were to become limestone. By and large, however, most of the northwestern part of Nevada is cave-less. What a pity.

Lehman Cave photo by Gretchen Baker

Lehman Cave photo by Gretchen Baker, NPS

About 20 million years ago the Sierra Nevada to the immediate west rose to nearly two miles in height. This effectively shut off the moisture-laden winds from the Pacific Ocean and started the desertification of the bucolic central Nevada terrain of what was to become the Great Basin. The Sierra Nevada, itself a microplate some 400 miles long and nearly 140 miles wide, was then worn down to modestly high hills until a renewed uplift, perhaps 2 to 3 million years ago, again pushed these rocks up to about three miles in elevation.

Once western North America stabilized just a bit more and Nevada took a breather, descending films of ground water sank into the thin soils. Soil bacteria produce about 100 times the amount of carbon dioxide than is present in the air we breathe and thus the downward seeping ground water became carbonic acid, a chemical soup in which limestone is very soluble. The weak acid slowly dissolved out the limestone along nearly-vertical joints and gently inclined bedding planes. At first isolated chambers and pockets were formed because of the reduced amount of ground water available. These embryonic caves formed close to what was then the "water table" - really a misnomer since there is no classic water table in karst areas, only isolated reservoirs, standpipes, and tubes so to speak. In any case the caves being formed were largely isolated and not integrated into networks of passages. The pockets and isolated chambers then sat idle, being filled with ground water fully saturated with dissolved calcite and with nowhere to go.

Gradually the surface was eroded down, streams cut their canyons deeper, and what ground water there was slowly drained away to the lower, gravelfilled inter-montane basins. This allowed fresh acid ground water to percolate in, dissolving larger rooms and more passages. In some cases, geothermal heat warmed the ground water and aided in dissolving the caves, but in only a few instances. The major rooms in many of Nevada's caves most probably started as large, isolated chambers. Gradually these coalesced into irregularly shaped rooms with fairly large vertical extent. These rooms often roughly parallel the range fronts because the cave-guiding faults and joints approximately parallel the range fronts themselves. Cave Valley Cave, for instance, roughly follows the trend of its enclosing limestone hill, itself roughly parallel to the faults bounding Cave Valley and the bordering South Egan and Schell Creek Ranges. The same may be said for the lofty passages in Whipple Cave to the south and the group of major caves in the Smith Creek area.

In other locations, the surface drainage has played a major role in guiding the development of caves. In Baker Creek at Lehman Cave, for instance, the cave passages are a direct result of continued solution of the limestone adjacent to and under the bed of Baker Creek.

Other caves apparently reflect their development as large "pores" in the massive limestone of their respective enclosing mountain ranges. Rose Guano Cave, Whipple Cave, and Mining Canyon Cave are examples of this seemingly random development (but we add that detailed studies of many of these caves have not been made and there may be other factors influencing their development).

Still other Nevada caves are the result of solution of limestone along a relatively narrow pathway. Karst springs such as Ragged Cave in Eastern Nevada and Deer Spring Cave in the Charleston Range in the far western edge of the state owe their development to a network of cracks and fissures that funnel ground water to a single outlet. Model Cave near Lehman Cave appears to have also been a fully water-filled pressure tube cave that only recently has been faulted open. Abundant scallops, oval cross section passages, and other features show its initial development fully under the water table followed by faulting open and draining to form a seasonally flooded lengthy cave partly still partly filled with its much older sediment fill.

Beware Cave at the Nevada-Utah border is another special case cave. It has formed inside a modestly large deposit of calcite travertine. The thermal water has ascended along a fault, bringing dissolved calcite with it (this fault most likely is the same which played a major role in the location of Gandy Peak proper that holds both Crystal Ball Cave and several other smaller caves). This pinnacled block of limestone may either be an up-faulted outlier of the Snake Range or possibly a large landslide block of enormous proportion that has slid east from the main range. In any case the warm, calcite-saturated waters have formed a lovely little cave as an outlet for a major, warm water karst spring.

Photo by James Rice

Spring photo by James Rice

Thus many of Nevada's caves are relatively newly formed. We do not have any good dates for most of this solution, but we do know that at nearby Lehman Cave, its passages are essentially horizontal and not affected by the roughly 2 million years ago uplift episode of the enclosing Snake Range. This was the time of the last major episode of faulting and drastic uplift to the eastern Great Basin ranges in the immediate cave area, although slow uplift continues today. Since many of the eastern Nevada caves also lack any systematic, east-west tilting with side passage being either above and below the main cave's elevation, it may be assumed that they, too, are less than 2 million years old.

Uranium-thorium radiometric dates from a pair of stalagmites from Lehman Cave obtained by geologists in 2015 show a spurt of growth between 16,400 and 3,800 years ago with a hiatus between 12,700 and 8,200 years ago. These growth spurts may reflect the colder and thus wetter environments of the Older Dryas and Younger Dryas time intervals that centered about 14,000 and ~12,900-11,700 years ago. The Lehman stalagmite record also shows a drying trend after about 8,200 years ago. These dates agree well with those of other studies showing the general drying of the Great Basin during the past at least 2 million years. So we may conclude that, as in the case of Lehman Cave, most of the decoration of many of eastern Nevada's caves started forming in the late Pleistocene Epoch and continued forming in the Holocene Epoch; i.e., between approximately 130,000 years ago and the present. This dates the actual formation of these caves to well before about 130,000 years ago since the cave needs to be present before being decorated.

Photo by John Woods

Several cavers/graduate geology students/members of the now inactive Stanford Grotto spent the entire summer of 1952 studying the caves of the southern Sierra Nevada and Nevada. They made excellent observations on many of the Nevada caves. Lacking the knowledge we now posses because of radiometric dating and other sophisticated age dating methods, some of their speculations are somewhat wide of the mark. However, being keen observers, they, too, deduced that some of the largest caves in eastern Nevada may be as old as Pliocene and were subsequently modified in the wetter intervals of Pleistocene and Holocene Epochs, i.e., between about 5 and 1 million years ago. Thus until someone comes forth with a large bag of gold coin to pursue this facet of Nevada's natural history, we will have to speculate as best as we can.

ELY, NV WEATHER

Tonight

Partly Cloudy Partly cloudy, with a low around 32. South wind 20 to 25 mph, with gusts as high as 40 mph.

Sunday

Isolated Showers And Thunderstorms then Isolated T-storms Isolated showers and thunderstorms between 11am and 5pm, then isolated thunderstorms and scattered rain and snow showers. Partly sunny, with a high near 55. South wind 10 to 20 mph. Chance of precipitation is 30%.

Sunday Night

Isolated T-storms Isolated thunderstorms and scattered rain and snow showers. Mostly cloudy, with a low around 29. West northwest wind 5 to 10 mph. Chance of precipitation is 40%. New snow accumulation of less than one inch possible.

Ward Charcoal Ovens

Ward Charcoal Ovens

Located just south of Ely, Nevada, the Ward Charcoal Ovens are associated with the silver mining ghost town of Ward. They were built in 1876 by itinerant Italian masons known as carbonari. Charcoal prepared in the ovens was used in the nearby silver smelters.

Symposium Merchandise

h2go Essen Vacuum Food Container

It's a double-wall, stainless steel, 17 oz capacity thermos from h2go®. This thing is more rugged than your cave pack! We've been trying to beat up the manufacturer's sample, but it keeps winning. Hot things stayed hot, cold things stayed cold... and ours will have cool cave art printed on it.

RECENT NEWS

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JUNE 29, 2023
NCKMS Steering Committee Chooses Ely, Nevada as Host City for 2025 Symposium
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Lily the Cave Bear

Cave Bear - Arctodus simus

Ely, Nevada's White Pine Public Museum features the skeletal model of a cave bear (Arctodus simus) that was discovered in a nearby cave in 1982. This extinct species inhabited North America during the Pleistocene epoch from about 1.8 Mya until 11,000 years ago. It was the most common early North American bear and is considered one of the largest known terrestrial mammalian carnivores.

The museum's collections also include an extensive mineral display of copper ore samples, petrified woods, and fossils of ancient marine life.

Registration

Advance registration for the 2025 symposium is expected to open in mid-2024. We will send an email to past attendees when that system comes online.

Feel free to join our mailing list if you would like to receive occasional updates on our plans.

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