The following posting is an update from the Oceans Melting Greenland mission. It has been sourced via materials provided by NASA. There is an associated paper published within Science Advances.
Scientists with NASA’s Oceans Melting Greenland mission are probing deep below the island’s warming coastal waters to help us better predict the rising seas of the future.
Greenland’s melting glaciers, which plunge into Arctic waters via steep-sided inlets, or fjords, are among the main contributors to global sea level rise in response to climate change. Gaining a better understanding of how warming ocean water affects these glaciers will help improve predictions of their fate. Such predictions could in turn be used by communities around the world to better prepare for flooding and mitigate coastal ecosystem damage.
Measuring Each and Every Fjord
But researchers have long lacked measurements of the depths of the fjords along Greenland’s craggy coast. Without this information, it’s extremely difficult to arrive at a precise assessment of how much ocean water is being allowed into the fjords and how that affects glacier melt. By measuring their fjords one by one, a new study published in Science Advances has quantified, for the first time, how the warming coastal waters are impacting Greenland’s glaciers.
The Oceans Melting Greenland Mission
For the past five years, scientists with the Oceans Melting Greenland (OMG) mission have been studying these marine-terminating glaciers from the air and by ship. They found that of the 226 glaciers surveyed, 74 in deep fjords accounted for nearly half of the total ice loss (as previously monitored by satellites) from Greenland between 1992 and 2017. These glaciers exhibited the most undercutting, which is when a layer of warm, salty water at the bottom of a fjord melts the base of a glacier, causing the ice above to break apart. In contrast, the 51 glaciers that extend into shallow fjords or onto shallow ridges experienced the least undercutting and contributed only 15% of the total ice loss.
“I was surprised by how lopsided these findings were. The biggest and deepest glaciers are undercut much faster than the smaller glaciers in shallow water, in other words, the biggest glaciers are the most sensitive to the warming waters, and those are the ones really driving Greenland’s ice loss.”lead author Michael Wood, a post-doctoral researcher at NASA’s Jet Propulsion Laboratory in Southern California, who began this research as a doctoral student at the University of California, Irvine.
In the case of Greenland’s glaciers, the bigger they are, the faster they melt. And the culprit is the depth of the fjord they occupy: Deeper fjords allow in more warm ocean water than shallow fjords, hastening the undercutting process.
Undercutting and Calving of Greenland Glaciers
Greenland is home to one of Earth’s only two ice sheets.The ice there is over 2 miles (3 kilometers) thick in places. At the edges of Greenland, the vast glaciers extending from the ice sheet travel slowly down valleys like icy conveyor belts, which pour into the fjords and then melt or break off (or calve) as icebergs. The ice is replenished by snowfall that is compressed over time into the ice pack.
If the ice sheet were in balance, the amount of snow accumulating on the top would roughly equal the ice lost from melt, evaporation, and calving. But previous observations have shown that the ice sheet has been out of balance since the 1990’s: Melt has accelerated and calving has increased. In other words, the rate of ice being lost to the ocean is exceeding the supply from the ice sheet. This is causing the ice sheet to shrink and the glaciers to retreat toward land.
The main cause of such glacier retreat is the process of undercutting, which is driven by two factors: the amount of meltwater flowing from the glacier and the warm layer of salty water at the base of the fjord. During the summer months, increasing air temperatures heat the glacier’s surface, creating pools of meltwater. These pools leak through the ice and flow from the glacier in rivers below the surface. As the meltwater flows into the sea, it encounters the warmer salty water at the bottom of the fjord.
Glacial meltwater doesn’t contain salt, so it is less dense than saltwater and thus rises as a plume. The plume drags the warmer ocean water into contact with the glacier’s base. The amount of undercutting depends on the depth of the fjord, the warmth of the ocean water, and the amount of meltwater flowing out from beneath the glacier. As the climate warms, the amount of meltwater will increase and the ocean temperature will rise, two factors that boost the undercutting process.
Animation: How a Glacier Melts
What do these findings tell us?
These findings suggest that climate models may underestimate glacial ice loss by at least a factor of two if they don’t account for undercutting by a warm ocean.
The study also lends insight into why many of Greenland’s glaciers never recovered after an abrupt warming of ocean water between 1998 and 2007, in which ocean temperature increased by nearly 2 degrees Celsius. Although ocean warming paused between 2008 and 2017, the glaciers had already experienced such extreme undercutting in the previous decade that they continued to retreat at an accelerated rate.
“We have known for well over a decade that the warmer ocean plays a major role in the evolution of Greenland glaciers, But for the first time, we have been able to quantify the undercutting effect and demonstrate its dominant impact on the glacier retreat over the past 20 years.”OMG Deputy Principal Investigator Eric Rignot of UCI and JPL, which manages the mission.
Into the Icy Depths
Now in its sixth year, the OMG mission has carried out the mammoth task of measuring ocean temperature and salinity around the entire coast of Greenland. Each summer since 2016, the team has spent several weeks dropping between 250 and 300 probes from an aircraft to measure how water temperature and salinity change with depth while mapping the depth of otherwise-inacessible fjords.
This data complements other surveys of the region – including OMG measurements via boat (which began in 2015) and observational data collected from the Landsat satellites from NASA and the U.S. Geologic Survey – and builds on a growing body of glacier research on ice-ocean interactions. During this time, the OMG team has been able to gain a detailed view of how quickly the 226 glaciers studied are melting and which are retreating the fastest.
What next for OMG?
OMG is planning its campaign for the summer of 2021. The team hopes that the ongoing measurements of ocean conditions will be invaluable for refining predictions of ice loss, ultimately helping the world prepare for a future of rising oceans.
“When the ocean speaks, the Greenland Ice Sheet listens, This gang of 74 glaciers in deep fjords is really feeling the influence of the ocean; it’s discoveries like these that will eventually help us predict how fast the ice will shrink. And that’s a critical tool for both this generation and the next.”OMG Principal Investigator Josh Willis, also of JPL.
Further Reading on the Oceans Melting Greenland mission
For more information, visit:
You can find the full open access paper here …
- Science Advances (Jan 2021) – Ocean forcing drives glacier retreat in Greenland
Details from the Published paper
Mini Glossary: TF = Thermal Forcing – Basically warm ocean eating away at the glaciers.
Fig. 1 Regional comparison of ocean TF and glacier retreat during 1992–2017.
The reconstruction of ocean TF (°C)—the depth-averaged difference between the in situ water temperature and the salt- and pressure-dependent freezing point of seawater—and cumulative glacier retreat (Qˆr, square kilometer) is shown for …
- (A) all 226 marine-terminating glaciers (red; ±1σ of all regions), respectively
- (B) northwest (NW)
- (C) central west (CW)
- (D) southwest (SW)
- (F) north (N)
- (G) northeast (NE)
- (H) central east (CE)
- (I) southeast (SE) Greenland.
Linear regressions in TF through stable, warming, and cooling periods are identified as three thin black lines.
(E) Sample areas (thick black, numbered by region) used to evaluate TF in seven regions, with major ocean currents (white), overlaid on a reconstruction of potential temperature at 257-m depth from the MITgcm ocean model for November 2005 (3). IC, irminger current; WGC, west greenland current.
Fig. 2 Schematic diagrams for four major categories of marine-terminating glaciers, with cold, fresh polar water (PW) on top of warm, salty AW.
- (A) Glaciers in deep fjords with warm AW (DW) that undercuts the glacier face to affect basal resistance.
- (B) Glaciers with temporary floating extensions on a shallow ridge (SC), for which undercutting does not affect basal resistance.
- (C) Glaciers standing in shallow, cold waters (SC).
- (D) Glaciers develop long (>10 km) floating ice extensions (FE). Note that glacier and bed elevations, expressed in meters above sea level (m.a.s.l.), are approximations provided for illustration.
Fig. 3 Spatial distribution of glacier retreat and categorization.
Greenland glaciers (226) are classified by bathymetry and water properties as …
- deep and warm (DW; blue/white circle),
- calving on a ridge (CR; yellow circle),
- shallow and cold (SC; brown circle),
- terminating in a FE (gray circle);
- and by those with sustained retreat (SR; green circle) or NC (red circle).
Circles are proportional to the grounded ice loss in square kilometer for 1992–2017, with blue for undercutting versus other ablation processes on DW glaciers. ΔTW and ΔTC are net changes in ocean TF during the 1998–2007 and 2008–2017 periods, respectively. Background ice velocity map is from (35), and bathymetry is from (19).
Fig. 4 Summary of cumulative anomalies at the glacier terminus for ten examples.
(A to J) Example glaciers for the seven regions showing time series of observed ice front retreat,
- Qˆr(black), retreat induced by surface thinning,
- Qˆs (red), and cumulative anomalies in undercutting by the ocean
- Qˆm (blue) and in ice advection,
- Qˆf (green), for 1992–2017.
Second and fourth columns show the ice front location color coded from 1992–2017 overlaid on Landsat 8 imagery or bed elevation. Note that the vertical axis is scaled differently for each example.