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The Coming Decline…of Mountains

Some years ago, Mt. Elbert jumped from 14,433′ to 14,440′ above sea level. Some Coloradans hope this might be enough to push it past Mt. Whitney in California, but that peak too rose up, from 14,494′ to 14,501′. The change was because of the shift from the National Geodetic Vertical Datum of 1929 (NGVD29) to the newer (and presumably more accurate) North America Vertical Datum of 1988 (NAVD88). While the change did nothing for the local relative elevations (Mt. Massive, for instance, remained 12′ lower than nearby Mt. Elbert), there were some relative changes at the scale of the country.

The datum can be thought of (and is usually stated as) where sea level would be, though technically this isn’t quite true. Thus a change in the datum came about because of a change in the underlying estimate of where sea level was.  As you might well imagine, sea level is not easy to divine here in Colorado, but measurements with satellites as well as lots of surface surveys provided a lot of information.

However, it has turned out that there were some mistakes in NAVD88. Tide gauges on the West Coast were computed to be as much as 1.25m above actual sea level. NGVD29 was tied to a number of tide gauges, but NAVD88 was hooked in from one in eastern Canada. The result is that the datum differs from estimates of the geoid:

NAVD88Error

Error in the NAVD88 datum (purple areas are currently considered lower than NAVD88 calculates). From National Geodetic Survey.

So what is the solution? A new datum, of course: the North American-Pacific Geopotential Datum of 2022 (NAPGD2022). And while this is still being finalized, we have some idea of what the new datum will look like:

NAVD88Adjustment

A sharp eye might see that Mt. Whitney might decline by 0.75m (2.5′) while Mt. Elbert might only go down 0.5 m (1.6′). So Whitney (maybe 14,499′) will still be safely above Elbert (14,439?’).  But all the T-shirts and little fake geodetic monuments you can buy will change….

At the same time, there are changes in the horizontal NAD83 datum (the new one is NATRF2022) of a meter or two; both new datums will now move with the continent as geodesy finally has to deal with plate tectonics, post-glacial rebound and other assorted changes…

P.S. this change won’t deprive Colorado of any of its 14ers…but while it would seem peak 13,001 is at risk of dropping out of the list of 13ers, that elevation was an NGVD29 elevation and so was probably more like 13,008 in NAVD88…

Slab Tectonics?

So Howard Lee over at Ars Technica took a swing at how our understanding of global tectonics has been changing over the past 40 or 50 years and wrote a lengthy article on it.   It is full of quotes and assertions that really don’t hang together very well, making a certain geophysicist kind of grumpy.  It doesn’t seem that any of the scientists quoted were really saying anything wrong, but the assembly in the article, which doesn’t seem to recognize the discrepancies nor fully master the techniques being used, can lead to a sense of “WTF?”

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How to mislocate an earthquake [nerdy]

One of the bread-and-butter things seismologists do is locate earthquakes. There are kind of two main flavors of this: one is global and the other is local/regional.  GG doesn’t do global relocations (but will point out that depth of such locations often relies on the presence of depth phases like pP reflections from the surface or the relative strength of surface waves) but has done local event locations.  And there are gotchas out there that often aren’t as appreciated as they should be because all too often data is pitched into an inversion code and the resulting output is accepted as correct.

We’ll start with some simple things and move into somewhat complex stuff a bit but will stop short of the really ugly problems of locating events in a 3-D structure that is in part determined by those same travel times.

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Getting Colorado High: So What?

So in the previous two installments, we reviewed ideas for how the High Plains got so high and some of the observations out there that bear on this question. Beyond satisfying some curiosity, what does this do for earth science?  Why pay money to do this?

Let’s consider three outcomes: that the High Plains gained their elevation by the end of the Laramide orogeny (say, 40 Ma), that they gained their elevation after the deposition of the Ogallala Group (say about 5 Ma), and that they were high, went down, and rose again. Read More…

Path to Isostasy, Crustal Edition

We’ve discussed isostasy a few times here, but today let’s stand back and ask the question, how do we determine what has led to the creation of isostatically supported topography? We will for today put aside the discussions of dynamic topography and just concern ourselves with isostatically supported topography, which seems likely to describe much of the US Cordillera. For this post, we’ll just focus on the crustal part of the problem, leaving the mantle for another day.

OK, first up is that isostasy means that the integral of density from the surface to some depth of compensation (usually somewhere in the asthenosphere) is constant. So how do we get at density at such great depths?  At first blush you might think “gravity” as that is the geophysical observable produced by mass. The problem is that gravity is non-unique: you can recreate any gravity field by having a thin surface layer varying in density. Gravity gradients tell you of the maximum depth an anomaly can lie, and the integral over a broad region tells you of the total mass surplus or deficit relative to some reference. Those integrals support isostasy, but the gradients are tough to work with because isostasy is only thought to work well at long enough wavelengths that the strength of the lithosphere becomes irrelevant.  So in essence you need to smooth gravity out to appropriate wavelengths–and once you do that, the depth limits in the raw gravity are pretty much gone.

So with gravity being relatively useless, where do we go? Keep in mind that we’ll be wanting to compare two columns to be able to discern what happened at one column relative to the other to produce a difference in elevation.

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A Go at Geoid (technical)

Consider for a moment the geoid, which is the difference in elevation between a reference spheroid and an equipotential.  The geoid has lots of neat properties, among them being directly related to the gravitational potential energy in the lithosphere. It is sensitive to density variations at great depths and so can give us insight into deep earth processes.  But there are some issues that casual readers of papers using geoid might want to be aware of.

Geoid has long been recognized as having a sensitivity to greater depths than gravity, but this is a mixed blessing as density variations far below the asthenosphere can affect the geoid, complicating a lithospheric interpretation. The most common approach is to filter the geoid to eliminate long wavelengths that are most sensitive to deep structure–but these same wavelengths are also sensitive to the difference between continents and oceans.  In the western U.S., the look you get from the geoid depends on how you filter it.  For instance, these are two images of the geoid, one as published in Jones et al., Nature, 1996, and the other with a different filter.

Geoid7-11-JonesEA96Geoid10-15-JonesEA96

The clearest difference is at the right, where the solid zero line has moved a lot, but also note that the scale of the color bar has changed.  It can be a bit hard to compare these, so another way of looking at it is to plot some points from each against each other:

WUS_GeoidByProv

Geoid by province in the southwestern U.S.; error bars reflect scatter in the subset of points within each province used to make this plot (points were where seismic structures were located in Jones et al., 1996)

The diagonal line would be where points would plot if both filters yielded the same values. Clearly the southern Rockies (SRM) pick up a lot of power in the degree and order 7-10 range compared with, say, the Sierra Nevada (SN). If interpreting this for potential energy, at D&O >7 taper to 11 the western Great Plains (GP) would have a positive GPE and would be expected to have normal faulting, but at D&O >10 taper to 15 it would be quite negative and you would expect to have compressional stresses and possible reverse faulting.

(Beyond the issues with the edge of the filter is the nature of the taper–a brute force cutoff can produce some artifacts you might not want to interpret.)

Anyways, what is the appropriate filter?  There is no simple answer for three reasons.  One is that the maximum depth you might care about probably varies across the region so a filter that cuts off in the asthenosphere in one place might also cut off the lower lithosphere in another. Another is that there is significant shallow power in the longer wavelengths/lower orders: continent/ocean boundaries have some real power in low degrees and orders. So when you filter out the long wavelengths, you can be removing shallow signal as well as deep signal. The third is that the sensitivity with depth is gradational, so a filter won’t fully cut off greater depths unless there is reduction in power from shallower ones.

(If you are wondering, in the paper we chose D&O 7-11 as the most appropriate filter for our purposes).

So be cautious when a filtered geoid is presented as a purely lithospheric signal, for it could be contaminated with deep sources or cutting off shallow ones.

EarthScope and Tectonics

Recently NSF’s EarthScope program office put out a media announcement with the top ten discoveries they attributed to the soon-to-end program. (EarthScope, for those unfamiliar with the program, originally had three main legs: the Transportable Array (TA) + Flex Array collection of seismometers, the Plate Boundary Observatory (PBO) network of GPS stations, and the San Andreas Fault Observatory at Depth (SAFOD), a drill hole through the fault).  What struck GG about this collection was just how little we learned about tectonics, which was a selling point of sorts for the program prior to its start.

Now some of the “discoveries” are not discoveries at all–one listed is that there is a lot of open data.  Folks, that was a *design*, not a discovery. A couple are so vague as to be pointless–North America is “under pressure” and there are “ups and downs” in drought–stuff we knew well before EarthScope, so these bullets give little insight to what refinements arose from EarthScope. And then the use of LIDAR to look at displacements of the El Mayor-Cucapah earthquake was hardly a core EarthScope tool or goal even as the program might have contributed funds. So the more substantive stuff might amount to 5 or 6 points.

Arguably PBO has more than delivered and SAFOD disappointed, but GG would like to consider the TA’s accomplishments–or non-accomplishments. TA-related “discoveries” in this list are actually a single imaging result and two technique developments (ambient noise tomography, which emerged largely by happy coincidence, and source back projection for earthquake slip, which is largely a continued growth of preexisting techniques). So in terms of learning about the earth, we are really looking at one result worthy of inclusion.

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