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Multi-scale Sources of Precipitation Predictability in the Northern Great Plains

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05 December 2023

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06 December 2023

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Abstract
This study leverages the relationships between the Great Plains low-level jet (GP-LLJ) and the circumglobal teleconnection (CGT) to enhance the 30-day rainfall forecast skill in the Northern Great Plains (NGP). The assessment of 30-day simulated precipitation using the Climate Forecast System (CFS) is contrasted with the North American Regional Reanalysis, searching for sources of precipitation predictability associated with extended wet and drought events. We analyze the 30-day sources of precipitation predictability using (1) the characterization of dominant statistical modes of variability of 900-mb winds associated with the GP-LLJ, (2) the large-scale atmospheric patterns based on 200-mb geopotential height (HGT), and (3) the use of GP-LLJ and CGT conditional probability distributions using a continuous correlation threshold approach to identify when and where the forecast of NGP precipitation occurs. Two factors contributing to the predictability of precipitation in the NGP are documented. We found that multi-scale geospatial interactions occur at the daily and sub-seasonal time windows. The CFS reforecast suggests that the ability to forecast sub-seasonal precipitation increases in response to the enhanced simulation of the GP-LLJ and CGT. Finally, the multi-dimensional analysis of covariance reveals that high-precipitation forecasting skill is associated with a better prognostic of GP-LLJ and CGT.
Keywords: 
Subject: Environmental and Earth Sciences  -   Atmospheric Science and Meteorology

1. Introduction

Six major U.S. climate-model development institutions (NOAA GFDL, NCAR, NASA GISS, DOE ACME, NASA GMAO, and NCEP CFS—list of acronyms in Table S1) have coordinated the efforts that could be translated into a better understanding of sources of climate predictability in almost a decade [1,2]. The motivation behind these modeling efforts is to improve operational sub-seasonal forecasts (10 to 60-day); however, climate predictability at such temporal lead times is still a major challenge [4,5,6,7]. Of particular interest is the sub-seasonal forecasting skill and predictability of precipitation in the United States Northern Great Plains (NGP) during late spring and early summer, May through July [8]. During this season, extended precipitation event, or their absence, may lead to natural disasters such as the 1993 flood in the Midwest or the 1988 and 2012 droughts (Figure 1 and Figure 2), considered some of the costliest events in the history of the United States with estimated damages of 20 and 40 billion dollars [9,10]. Losses in the NGP included drops in corn yields of about 30% for Nebraska, Iowa, Minnesota, and Illinois, which affected local farming and regional economies [11]. These states lie in the U.S. Midwest, where the corn economy is valued at about 50 billion dollars [12]. Also, this region is considered a production hub for corn, soybean, and cattle and halves in the United States [13,14], making climate diagnostics and prognostics key to food and biofuel production and water resources security [15,16,17,18,19,20,21,22].
Precipitation variability in the NGP has been related to the spatial and temporal variability of the Great Plains low-level jet (GP-LLJ) [24,25,26]. During the summer season, NGP precipitation and the GP-LLJ are linked through the transport of moisture from the Gulf of Mexico, the region's primary moisture source. The GP-LLJ can be identified using wind data from rawinsonde stations [24] and wind profiler observations [26]. Wind at 900-mb is in several retrospective reanalyzes [27], such as NCEP-NCAR [28] and the North American Regional Reanalysis (NARR)[29]. The GP-LLJ, which has its maximum annual cycle during May through July (with a peak in July), allows an efficient moisture transport through an extensive plains surface center at 900-mb and along 95ºW [27].
Rainfall variability of the northern Great Plains is also linked to large-scale atmospheric teleconnections [27,30,31]. At 200 mb, the association between the GP-LLJ index and geopotential height (HGT) shows a positive strength center over Tennessee, acting over the country's eastern half, and a Rossby-wave train pattern [32]. This geopotential-height pattern matches the interannual variability characteristic of the atmospheric circumglobal teleconnection (CGT) [33]. Observational and modeling indicate that CGT affects summer precipitation in the United States [30,31]. The CGT pattern with one center of action located over North America is essential in driving the variability of summer precipitation over the Northern Hemisphere [33]. The authors [30] showed that the CGT pattern affects the rainfall distribution during the summer. This evidence can be a source of predictability for precipitation in North America and East Asia. Further, [31] found two CGT climatic modes that affect North America's summer precipitation in the Southern and the Northern Great Plains. The pattern in the Northern Great Plains is responsible for 16% of the early summer (June-July) variability, as evidenced by the application of Empirical Orthogonal Function (EOF) analyses [30]. These authors showed that the maximum strengthening of the CGT during July matches the maximum transport of low-level moist air from the Gulf of Mexico into the Great Plains. How these two components of U.S. climate variability (the CGT and the Low-Level Jets) affect the predictability of summer precipitation over the NGP region is a major interest of this study.
Although NGP precipitation variability has been extensively studied for several decades [24,26,27], the predictability in the sub-seasonal range is still a challenge [34,35]. The authosrs [36] reported the limited skill of the Climate Forecast System (CFS) to predict rainfall at ranges higher than 30 days. After many improvements on CFS version 2, they discussed that it is as good forecasting as its predecessor version 1. However, at a 15-day range, they found a significant improvement in precipitation forecast from CFSv1 to CFSv2, which is attributed to the improved initial state in the tropical atmosphere. A multi-model ensemble prediction seems to be a promising approach, at least for some variables such as sea surface temperature [3,36], but comparisons among several models from major national modeling centers and CFS reveal a similar skill for precipitation [36]. Further understanding of the regional-to-global modes of variability, such as the GP-LLJ and CGT, and their interaction can help improve sub-seasonal forecasts, especially in agricultural landscapes reliant on precipitation forecasts for crops.
The following questions arise: How strong is the link between the GP-LLJ and CGT in a modeling framework—concerning the evolution of summer precipitation over the Northern Great Plains? Furthermore, how does precipitation predictability vary when the internal dynamics of a GCM capture these two modes of climate variability? In other words, whether the interaction between the GP-LLJ and CGT can influence precipitation predictability within a prognostic 30-day range. We hypothesize that the forecast skill of precipitation over the NGP can be better assessed if GP-LLJ and CGT's patterns of variability—at the daily-to-sub-seasonal and daily scales—are adequately simulated by the model used. We consider that the regional scale of the GP-LLJ combined with the large-scale circulation of the CGT could reveal the underlying mechanisms responsible for the improvement of sub-seasonal predictability in the NGP. The objectives are three-folded: (1) Estimate the GP-LLJ and CGT indices based on NARR and CFS diagnostic and CFS forecast products for at least 30 years; (2) Estimate the correlation threshold to assess the unconditional and conditional causality between NGP precipitation and the GP-LLJ and CGT indices; and (3) evaluate the 30-day forecast skill of the CFS-based daily precipitation forecast products for NARR data using the conditional association between NGP precipitation and the GP-LLJ and CGT indices. The lead time of 30-day length was selected based on the CFS's reported limited 20-day forecast skill [36]. Then the performance of CFS-based precipitation forecasts was then evaluated with the GP-LLJ and CGT simulation for the extended wet and drought events of 1993 and 1988, respectively.
The paper's organization is as follows: Section 2 describes the sources of data, Section 3 is the Methodology, which explains the estimation of GP-LLJ and CGT indices, correlation thresholds, and associations between precipitation estimates and the forecast products. Section 4 analyzes the results, and Section 5 discusses the paper's central thesis.

2. Materials and Methods

2.1. Data

Three data sources were selected to capture the observed, simulated, and forecasted atmospheric conditions that lead surplus or deficits of precipitation to the extended precipitation and drought events in the NGP.

2.1.1. Observed gridded precipitation products

Daily precipitation values from two datasets were used for climate diagnostics and CFS’s ability to simulate the sub-seasonal variability and predictability of precipitation over the Northern Great Plains region. (1) The observed precipitation at 1/16º spatial resolution [23]. This product was derived from approximately 20,000 NOAA Cooperative observed stations, gridded using the synergraphic mapping system method [38], and scaled on a monthly basis to match the long-term mean from the Parameter-Elevation Regressions on Independent Slopes Model (PRISM) [39]. (2) The Climate Prediction Center (CPC) Unified Gauge-Based Analysis precipitation data [40] was also used to compare with modeling simulation with a coarse resolution. CPC unified precipitation, in its native 0.25º x 0.25º resolution, covers the conterminous United States, and it has unified various CPC precipitation products. Both precipitation datasets were used at daily resolution and covered the Northern Great Plains.

2.1.2. NARR reanalysis

The NARR was used to validate the forecasts. The meridional wind at 900 mb (V900) was used to compute the GP-LLJ index, and HGT at 200 mb was used to calculate the CGT index (see below). The NARR integrates the assimilation of observed hourly precipitation [29], which becomes key at daily to sub-seasonal scales to identify the GP-LLJ and its atmospheric response at 200-mb geopotential height.

2.1.3. CFS

The retrospective and forecast CFS connected observations to modeling diagnostics and prognostics. The model skill assessment under known boundary conditions used the same variables from the global CFS retrospective reanalysis (CFS-RR) [41]. The CFS reforecast (CFS-R) skill assessment used similar fields as the CFS-RR dataset. Forecasts of 30-day precipitation were computed from the CFS reforecast [36] obtained from the National Centers for Environmental Prediction (NCEP) in its reforecast version. The CFS reforecast was from NOAA National Operational Model Archive and Distribution System (NOMADS) [42]. The 9-month CFS-R simulations are used from the existing period from 1982 through 2009. For all cases presented here, we took the 12Z initialization from May 1 through September 1 each year. We apply a similar analysis for CFS in forecast mode to assess the predictability skill. The approach explores whether the model using the same reanalysis as initial conditions shows an adequate representation of 30-day precipitation of the NGP associated with the dominant statistical modes of GP-LLJ variability.

2.2. Methodology

The GP-LLJ and CGT patterns of variability were obtained using EOF analyses on 900-mb meridional wind and 200-mb HGT, respectively. The correlations between precipitation and the GP-LLJ and CGT used the historical precipitation distribution and the meridional wind's temporal PC and the HGT fields, respectively (as observed in Figure 3).

2.2.1. The GP-LLJ index

Before assessing the predictability skill of the modeling products in forecast mode, we evaluated whether the CFS model using boundary conditions from the reanalysis version (CFS-RR) adequately represented the dominant statistical modes of GP-LLJ variability associated with NGP precipitation. The GP-LLJ temporal index was defined as the temporal Principal Component (PC) from 900-mb meridional wind during the summer season MJJA. We defined the spatial patterns as EOFs and the temporal patterns (or time series) as PCs [43]. The GP-LLJ is usually defined as the maximum wind frequency in a 95° to 100° west region on the Oklahoma-Kansas border at 37°N [24]. We followed a similar EOF approach described in [27,32], using the 900-mb meridional wind anomaly (ΔV) to assess the intraseasonal and interannual variability GP-LLJ. The GP-LLJ EOF analysis is applied over anomalies Δ V = V − V ¯ , where V ¯ = 1 n ∑ i = 1 n v i is the seasonal mean average of MJJA for each year. Thus, the analysis removed the seasonal mean, and the higher EOFs explain the sub-seasonal variability. EOF analyses characterize statistical modes of variability of the GP-LLJ [44]. GP-LLJ statistical modes of variability were obtained from both 1-day and 5-day time series sampling frequency over the domain (15°-50°N; 110°-75°W) for the sub-seasonal and interannual scales, respectively. Both daily and 5-day fields were previously band-pass filtered on the sub-seasonal scale (10- to 60- day). This band-pass filtering process was done for each year independently, using a length from May 1 through September 1. For the interannual variability, the 5-day sampling frequency was implemented after band-pass filtering for each year from 1982 to 2014. The filtering approach helped show whether the CFS-RR at the sub-seasonal scale could simulate the variability of the GP-LLJ as the first EOF mode described by the NARR. As in [27], the EOF1 and EOF2 show the GP- LLJ wet and dry modes of variability, respectively. The GP-LLJ index was defined as the temporal Principal Component (PC) of the NARR and the CFS from 900-mb meridional wind during the summer season MJJA. The spatial patterns in this paper were denominated as EOFs and the temporal patterns (or time series) as PCs [43].

2.2.2. The CGT index

The NGP precipitation response to upper-level atmospheric was evaluated using spatial and temporal correlations between the GP-LLJ temporal index and 200-mb geopotential height (HGT) anomalies. Also, the EOF analysis was applied on 200-mb geopotential height to identify the CGT large-scale atmospheric pattern linked with the temporal variability and spatial distribution of precipitation and the GP-LLJ. The spatiotemporal variation of the HGT and the CGT index were explored. The first pattern of variability emerged from the spatiotemporal variability of the CGT index, which was reconstructed by the HGT’s EOF2 and PC2 ( H G T ~ = E O F 2 × P C 2 ). The second pattern of variability emerged from the EOF1 of 10-60-day band-pass filtered HGT anomalies for all cases. These patterns of variability enabled the systematic evaluation of CGT as the dominant pattern of variability. The consequent correlations and EOF maps (see subsection 3.1) represent the spatial coherence of variability between observations and simulations, quantified by the spatial correlation between a limited domain.
  • Band-pass filter and power spectra
To systematically identify the CGT as the dominant mode of variability for each simulation, we applied a 10-60-day band-pass filter. This step guaranteed that EOF1 is CGT's dominant statistical mode for each forecast case within the sub-seasonal range. Following the method of [45], the band-pass filter created a variable transformation that employed a low-order Butterworth function to avoid the cutoff of the new time series when its length did not match the periodicity of the perturbation. The multi-taper method (MTM) identifies the significant spectral peaks computing the power spectra of temporal PCs and time series. MTM uses Slepian tapers (in this case, three tapers) to minimize spectral leakage, which results in a better trade-off between spectral resolution and statistical variance [46].

2.2.3. The thirty-day forecast of the CFS

Forecasts of 30-day precipitation were computed from the CFS reforecast [36]. The nine-month CFS simulations were used from the entire existing period from 1982 through 2009, which is the study period. A precipitation index (NGP precipitation) was computed to compare observed and simulated precipitation; the NGP precipitation is defined as the average precipitation over the NGP region (37.5°-45°N and 103°-90°W; see the box in Figure 1). We used the initialization at 12Z from May 1 through September 1 of each year for all the CFS cases presented here. To assess the predictability skill of CFS-R (in forecast mode), we used correlation analysis between observed and simulated GP-LLJ and CGT indices. The forecast skill of precipitation based on the GP-LLJ and the CGT indices was analyzed for a 30-day timespan. Here, both retrospective and reforecast simulations applied the same analyses. For the reforecast cases, we used a 90-day window to compute the statistical EOF of v-wind and HGT and ensure the integration of the sub-seasonal signals. We used the Pearson correlation between the CFS and observed NGP daily precipitation to evaluate the simulation skill.

2.2.4. Spatial and temporal attributions

The selected simulations of the GP-LLJ are those with statistically significant Pearson correlation coefficients between the GP-LLJ index of the NARR and the CFS-R for a 30-day lead time after the forecast initialization. We use the spatial correlation between the PC1 of the 900-mb meridional wind and the geopotential height to diagnose CGT at 200-mb. Changes in PC1 --in the 30-day Hovmoller diagram over the 40°-50°N latitudinal average-- support the statistical significance of the correlations as one of the criteria for patterns emergence from the principal components analysis. The second criterium is that the entire cases from 1982-2009 show the number of significant cases that occurred when the GP-LLJ and CGT are correlated with the already characterized patterns using the retrospective reanalysis cases. While the individual t-statistics test estimated the local significance at each grid point, the collective significance was evaluated using the method of field significance by [47]. The implementation of this method used randomization of every grid point, with 1000 Monte Carlo sampling, to compute a non-parametric distribution to assess the collective significance of the spatial patterns.
  • Correlation threshold selection
We selected the cases when the correlation was statistically significant and reached values higher than the estimated correlation threshold selection according to a non-parametric approach. The selection used a non-parametric distribution constructed by randomizing the original sequence of the time series using a bootstrap approach [44]. This distribution is the null distribution for testing the selected threshold. For two variables like GP-LLJ index and NGP precipitation, a bi-variated normal distribution is used:
f x , y = 1 2 π σ x σ y 1 − ρ 2 e x p − 1 2 ( 1 − ρ 2 )   x − μ x σ x 2 + y − μ y σ y 2 − 2 ρ x − μ x σ x   y − μ y σ y ,
which explores all the possible conditional realizations. The function f ( x , y ) is defined by the dimensional variables x and y; the mean μ x and μ y ; the standard deviations σ x and σ y ; and ρ is the correlation between x and y. Considering the hypothesis that overlapping GP-LLJ and CGT enhance the predictability of NGP precipitation, we use a multi-dimensional normal distribution of order three. In other words, this testing assesses the conditional probability of an event happening when another two events already occurred (e.g., a correlation higher than the threshold value between precipitation and GPLLJ and CGT). The multivariate normal distribution equation is below,
f x = 1 2 π K 2   d e t Σ e x p − 1 2   x − μ T   Σ − 1 x − μ ,
where μ is the K-dimensional mean vector of x , and Σ is the covariance matrix of x (Wilks 2011).

3. Results

3.1. Diagnostics of NGP precipitation, GP-LLJ, and CGT

The thesis presented here states that concurrent multi-scale climate phenomena improve the predictability of 30-day precipitation, or its absence linked to extended wet or draught phenomena in the NGP area. We tested the proposed sub-seasonal predictive framework for the precipitation events in 1993 and the consequent flooding event in the NGP. Also, the sub-seasonal predictability of precipitation deficit characteristic of droughts such as the 1988 event in the same area.

3.1.1. Geospatial precipitation pattern attributions

The spatial distribution of the GP-LLJ and CGT and the associated precipitation across the NGP area were analyzed using NARR data (Figure 3). The EOF analysis showed the spatiotemporal patterns of these variables for the 900-mb meridional wind (V900). The associated temporal PC1 is correlated with precipitation and 200-mb geopotential height. The V900 EOF1 shows the GP-LLJ and represents only 30% of the explained variance for 1993. The core of the GP-LLJ—along with Texas, Oklahoma, and Kansas—shows the same pattern as in other studies [24,27,32,43]. The spatial pattern of correlation (between precipitation and the V900 PC1, Figure 3b) shows a statistically significant positive relation in the north-central United States (Nebraska, Iowa, Minnesota, South Dakota, and North Dakota) with correlation values higher than 0.4 (p<0.05). This pattern coincides with the region of the maximum precipitation anomaly in Figure 1 and shows the association between the GP-LLJ and NGP precipitation. Simultaneously, the 200-mb HGT correlated with the V900 PC1 showed a high positive anomaly region over the Great Lakes, part of a wave pattern resembling the CGT. As noted by [30,31], this wave pattern reveals a large-scale linkage between continental patterns of precipitation anomalies and the variability of the westerly upper jet stream. The HGT pattern indicated by a complementary EOF analysis with 200-mb HGT anomalies (Figure 4 and Figure S1 with a global domain) illustrates the matching patterns obtained from a second approach using the EOF2. The complementary EOF analysis on the 200-mb HGT showed the CGT as the second dominant pattern (11% of explained variance). We evaluate next that CFS-RR, in a reanalysis mode, can reproduce a similar amount of variability for the GP-LLJ and the CGT.

3.1.2. Sub-seasonal modes of variability

The dominant temporal scales of the GP-LLJ, the CGT, and NGP precipitation were analyzed with power spectra to identify the temporal ranges of variability (Figure S2). Also, we suggest whether CFS-RR in a reanalysis mode can reproduce the GP-LLJ and CGT variability patterns. The GP-LLJ index (V900 PC1) had a dominant 6-day spectral signal, the GCT index (HGT200 PC2) showed a band at 10-60 days, and precipitation presented both. This result indicates that the dominant temporal modes vary in the daily (6 days) and sub-seasonal (10-60 days) scales, which are statistically significant at the 95% level of confidence (Figures S2 and S3). In Figure 5, the Hovmoller diagram for 1993 along 102º-90ºW depicts the relationship among precipitation (shaded), the GP-LLJ index (magenta line), and the CGT index (green line). It reveals the coherent variability of the GP-LLJ index at a high frequency and the CGT at a low frequency. Also, the three arrows in Figure 5 highlight CFS precipitation's forecast cases with a correlation above 0.35 (compared with observed precipitation). These instances coincide with the maxima of EOF's meridional winds at 900-mb and EOF's 200-mb geopotential height. This result illustrates cases where the magnitude of the GP-LLJ index and the phase transition indicated by the CGT index might play an essential role in the predictability skill of NGP precipitation.

3.1.3. Interannual modes of extended precipitation and drought

The analysis of EOF on the wind speed at 900mb on the CFS-RR and NARR datasets has shown the ability of both products to capture the underlying mechanisms of precipitation surplus and deficit in the NGP. The patterns of interannual variability of V-900 emerge from the EOF analysis applied to the NARR and CFS-R datasets for 1979-2010 and 1979-2014, respectively (these periods coincided with the observations). In Figure 6, the two dominant EOF1 and EOF2 spatial patterns obtained from NARR and CFS-RR indicate GP-LLJ's wet and dry climate regimes. In our analyses, the wet mode (EOF1) and the dry mode (EOF2) contribute 26% and 19% to the total variability, respectively, consistent with [32]. Additional analyses reveal that the CFS-RR contributes similarly to the total variability (Figure 6b). While the CFS-RR shows statistically similar results as the NARR, some minor differences between both products might be due to loading the two leading PCs. In the CFS-RR, the explained variance for the wet mode (EOF1) is 23%, and for the dry mode (EOF2), 18%. Based on the results above, the CFS simulates the GP-LLJ’s transport mechanisms of moisture from the Gulf of Mexico by enhancing it in the wet-EOF mode and suppressing it in the dry-EOF mode. The results indicate that the CFS-RR simulates the interdependence between NGP precipitation, the GP-LLJ, and the CGT, as in the 1993 flood and 1988 drought events. Sources of predictability of extreme precipitation might be more evident than those for drought. The latter indicates chronic or interannual water deficits, which require further analysis. The 1988 drought is explored using the EOF1 for 850-mb meridional wind (v850). The V850 correlated with precipitation (for coefficients between 0.45 to 0.55 during the 30-day range starting on July 15), confirming the dry GP-LLJ mode under drought (Figure S4). In the section below, we use a modeling framework in a forecast mode to illustrate how GP-LLJ and CGT are simulated for a 30-day precipitation forecast lead time.

3.2. Sources of NGP precipitation predictability

We further examined the relationship between GP-LLJ, CGT, and NGP precipitation in a forecast mode (CFS-R) at the daily and sub-seasonal scales. A particular interest was to identify whether precipitation predictability is enhanced when the CFS-R captures GP-LLJ and CGT during the initialization process. As a testing example, the forecast skill of simulated precipitation over the NGP for 1988 and 1993 was evaluated using temporal correlation for a 30-day timespan. The selection of cases was based on unidimensional and multidimensional distributions for continuous correlation thresholds. These analyses indicated the unconditional and conditional probability distributions for an improved predictive skill for NGP precipitation, GP-LLJ, and CGT. In the unidimensional case (Figure 7), a 0.4 correlation threshold at 95% suggests that the three variables are unlikely to be generated as a random process. When NGP precipitation is attributed to GP-LLJ or CGT, the bi-dimensional conditional distribution indicates that the probability of precipitation can be attributed to the occurrence of the regional-to-large scale climate phenomena presented here (Figure 8). The third case supports the central hypothesis of this study, meaning that the multidimensional conditional distribution –the rising probability of NGP precipitation when both GP-LLJ and CGT occur—likely leads to improvements in the predictive skill above a given correlation threshold (Figure 9).
Once the attributions are built and the correlation threshold selected (above 0.35), the correlation between NGP precipitation and the modeling and forecast products were evaluated. Table 1 shows the correlation between NARR (observed) and CFS-R (reforecast) precipitation for only eleven cases. Individual precipitation cases perform well (with r > 0.35) as some other cases show low correlation coefficients (Figure S5 shows two examples of simulated precipitation), like what [36] reported. Table 1 also shows the correlation between the CFS-R, GP-LLJ and the CGT for the observed and forecast precipitation datasets. The forecasting skill of the CGT was evaluated by correlating the HGT patterns from the 100º-60ºW region evolving 30 days, as shown in the Hovmoller diagram in Figure S6. This figure shows the temporal evolution of the dominant patterns of low and high values of HGT. The HGT emerged patterns based on EOF1 and EOF2 indicate that the CGT is the dominant mode of variability. The forecast-based patterns and phase transitions were comparable to those in NARR.
The relationship among the GP-LLJ, CGT, and NGP precipitation (Figure 5 and Figure S6) was expanded to the entire CFS-R simulations from 1982-2009 and synthesized in Figure 10 and Figure 11. These figures synthesize the 30-day correlation analyses of precipitation between the CFS-R and NARR for all the cases. The location of the boxes represents the forecast time of initialization and, inherently, the randomness of the cases. For MJJ only, we found that a total of 126 cases of NGP precipitation (Figure 10; 22.9% of the total analyzed) correlate (values higher than 0.35 and p<0.05) in the 30-day range. For an extended MJJA, 154 cases represented 21%, indicating no significant changes. From the first set, 40.5% (51) cases showed correlation values higher than 0.5. The threshold was selected based on [44] multidimensional probability distribution. This pool of cases (22.9%) was later used for assessing the role of the CGT and the GP-LLJ on NGP precipitation.
The 30-day correlation analyses of the GP-LLJ indices and 200-mb HGT anomalies (Figure 11a,b) were only shown for the cases in which simulated precipitation was significantly correlated (r>0.35; blue blocks in Figure 10), and only from May through July (MJJ). Categories for the cases were split into four groups according to the correlation value, such as r>0.35, r>0.45, r>0.55, and r>0.65. From a total of the 126 selected cases, 55 of them (43.6%) were able to simulate appropriately the GP-LLJ (Figure 11a) and 47 (37.3%) the CGT (Figure 11b), which is like what occurs in Table 1. These 43.6% and 37.3% represent the CFS's skill to simultaneously reproduce the GP-LLJ and the CGT, showing their importance to the predictability of NGP precipitation. This analysis's important caveat is that the selected cases were limited to 9% of the total possible in the CFS-R (121 cases). This sampling population could be fixed by including a multi-model analysis. However, this extra analysis is beyond the scope of this study.

4. Discussion

The predictability of precipitation has been evaluated by addressing two scientific questions: How strong is the link between the GP-LLJ and CGT in a modeling framework—concerning the evolution of summer precipitation over the Northern Great Plains? Furthermore, how does precipitation predictability vary when the internal dynamics of a GCM capture these two modes of climate variability?
The first question was answered by showing the GP-LLJ and the CGT's role in the variability of NGP precipitation at sub-seasonal and interannual scales. The link between the GP-LLJ, CGT, and NGP precipitation is strong, as shown by the NARR and CFS-RR using EOF analysis and Pearson correlation. In both reanalyses, the GP-LLJ contributes to the rainfall variability in the NGP at a daily scale (Figure S2). The EOF analysis of V900 for the NARR for 30 years identifies diagnostic patterns of spatiotemporal variability for the GP-LLJ that explain 26% of the variance; the same GP-LLJ pattern from the CFS-RR explains 23% of the variance. The EOF analysis on 200-mb HGT reveals the CGT as the second dominant pattern for the precipitation in the NGP, with an explained variance of 11%. We have found that the association between precipitation GP-LLJ and CGT occurs at the daily and sub-seasonal scales. Thus, NGP precipitation responds to regional-to-global moisture transport mechanisms in the lower troposphere. At the same time, these mechanisms are modulated by the CGT at the sub-seasonal scale, as shown on HGT anomalies caused by the upper-level jet stream.
The GP-LLJ, the CGT, and the NGP precipitation relationship identified in the CFS reanalysis define the metric to evaluate their role in a forecasting framework. Using a Hovmoller diagram of precipitation (Figure 5), this study depicts how the region's GP-LLJ peaks coincide with major convective storms. A correlation analysis between both gives a value of 0.4 (p < 0.05), which confirms previous research using alternative techniques [26]. Similarly, the CGT index reveals a statistically significant link with GP-LLJ with a correlation of 0.5 (p<0.05) between them. The GP-LLJ, CGT, and NGP precipitation relationship facilitates a metric to evaluate the 30-day predictability of precipitation. This analysis indicates how this relationship is maintained in space (by the CGT index) and time (by the GP-LLJ index). This process-based approach could incorporate the predictability of the dominant drivers of precipitation into the analysis. Further, the treatment of scale separation was beneficial when assessing the contribution of the dominant modes of climate variability at the global (CGT) scale.
For the second question, the 30-day NGP precipitation was evaluated in the context of the GP-LLJ-and-CGT relationship maintained in space and time. A study by [48] concluded that correct simulation of the GP-LLJ is necessary, but more is needed for adequately representing NGP precipitation. As hypothesized here, precipitation forecast skill increases in response to the enhanced simulation of the GP-LLJ and CGT at daily and sub-seasonal scales. The improved performance of the CFS precipitation in a forecast mode is due to the proper simulation of the GP-LLJ--CGT individual cases. At least 43% of the selected "good" cases outperform when they adequately represent the GP-LLJ and the CGT. Thus, it gives an objective process-based approach to quantify the role of these two modes of climate variability. Precipitation prediction is better when the relationship between these two climate variables is maintained.
The CFS, in a forecast mode, simulates limited cases of 30-day precipitation (r>0.5 [p<0.05]). This study has found that only 126 cases (22.9% of the total analyzed) were able to represent the 30-day precipitation variability with a correlation higher than 0.35 (p<0.05). In addition, from this group, 40.5% show correlation values higher than 0.5 (p<0.05); therefore, only 9% of the total simulated cases. A similar range of improvement can be found when the GP-LLJ and the CGT have the same thresholds. From the total 126 selected cases, 43.6% were able to simulate the GP-LLJ, and 37.3% of the CGT exceeded the threshold (r>0.35 [p<0.05]). These 43.6% and 37.3% of the cases demonstrate the importance of the GP-LLJ-and-CGT link for the predictability of NGP precipitation. A deeper analysis of the multidimensional covariance with a three-dimensional PDF also reveals that high precipitation correlation coefficients are associated with a better predictive GP-LLJ and CGT. Authors [27] also highlighted how essential the GP-LLJ is in the NGP precipitation. However, this research demonstrates that predictability is improved when the GP-LLJ and the CGT signals are adequately simulated. As the temporal variability of the CGT is higher in the range of 10-60 days, the CGT provides predictability in these cases. However, it is essential to consider the 6-day variability of the GP-LLJ, which plays a secondary role in extending the range of precipitation predictability to 30 days.
The GP-LLJ-and-CGT analysis suggests that its link is passed through the model during the initialization process. This model ability was confirmed when the CFS was evaluated using its reanalysis version. Perfect boundary conditions enable the modeling framework to efficiently simulate the GP-LLJ and CGT at the sub-seasonal and interannual scales. This outcome suggested that the initialization processes are critical. Thus, rainfall generation in the NGP in GCMs is not independent of the initial conditions. This condition may indicate substantial uncertainty in the modeling evolution of the GP-LLJ-and-CGT flux, but the large-scale flow well informs a few regional weather patterns.
Although the CFS-R, as analyzed by [36], showed meager predictability skill on average, this study showed that individual cases could reach higher skill levels when separated by how two significant drivers of precipitation are simulated NGP. Improved predictability of precipitation occurs when the GP-LLJ and the CGT are adequately simulated. In this context, predictability is limited to a few cases within what [49] call "windows of opportunities." This outcome could motivate researchers to explore further the initialization process of those dominant modes of variability or how the GP-LLJ-CGT link could be built into the internal dynamic of the modeling framework. Author [31] found that the CGT has two modes of variability that influence U.S. precipitation. This study encourages researchers to continue exploring how these two climate modes affect the predictability of precipitation. The combined use of these modes of variability could potentially help the improvement of predictive frameworks for water resources management and governance [19,50], phenotype predictability [22], and water supply for agriculture [51,52,53]; infrastructure risk and resilience [20,54]. Furthermore, the characterization of integration of variables such as soil moisture and soft computing can enhance the diagnostics and prognostics of extreme events associated with precipitation [55,56,57,58,59,60].

5. Conclusions

In conclusion, this study identifies the importance of the interaction between regional (GP-LLJ) and global-scale (CGT) sources on 30-day forecasted precipitation. Here, we documented how these two sources contribute to the predictability of precipitation in the NGP. However, we acknowledge that they can be limited in number, and more sources can still be there waiting for further analysis exploration. However, our approach shows that it can be expanded to a multi-variable problem (i.e., with machine learning). Although we have found that the interaction occurs at the daily (GP-LLJ) and the sub-seasonal (CGT) scale, we did not identify which source plays a leading role in predictability. That answer may be related to assessing the amplitude of forecasted precipitation (for example, extreme precipitation predictability differs from average precipitation). The analysis of the CFS forecast suggests that the ability to accurately forecast sub-seasonal precipitation increases when the simulations of the GP-LLJ and CGT are enhanced. These cases must be verified with other models or multi-model approaches (i.e., from the North American Multi-Model Experiment).

Supplementary Materials

The following supporting information can be downloaded at the website of this paper posted on Preprints.org, Figure S1: Spatial pattern of the Empirical Orthogonal Function mode 2 (EOF2) from 200-mb geopotential height anomalies (ΔHGT). The HGT is obtained from the Climate Forecast System (CFS) retrospective reanalysis. The EOF is calculated with daily fields from May 1 through September 1 (MJJA) of 1993, with explained variance of 6%; Figure S2: Multi-taper method (MTM) power spectrum of the temporal dominant Principal Components (PC) of both 900-mb meridional wind (V-wind PC1; a) and 200-mb geopotential height anomalies (ΔHGT PC2; b) for the daily period from May 1 through Sep1, 1993. MTM power spectrum of precipitation ([P]; c) for the northern Great Plains precipitation index averaged over the region defined at 37.5-45°N; 103-90°W (MW). The two superimposed lines are the levels of confidence at the 95% and 99%; Figure S3: Multi-taper method (MTM) power spectrum of 200-mb geopotential height (a), Precipitation (b), and meridional wind at 900-mb (c). The spectrum is calculated for several years indicated in the plot: 2010, 1993, 1998, 2008, and 2010. The time series of each field are average over different areas for precipitation (is 37-43N; 102-90W), HGT (40-60N; 90-60W), and V900 (25-40; 102-95W). The time series are daily for the period from May 1 through Sep1, 1993. The superimposed line is the levels of confidence at the 95% level of confidence for each case; Figure S4: Spatial pattern of the Empirical Orthogonal Function mode 1 (EOF1) from 850-mb meridional wind (V850mb). The V850mb was obtained from the Climate Forecast System (CFS) retrospective reanalysis (CFSRR). The EOF is calculated with daily fields from May 1 through September 1 (MJJA) of 1988. A correlation of 0.54 is found between the associated V850 PC1 and the analogous NARR PC1 for a 30-day length after Jul 15, this correlation is in the range [0.45, 0.55] as defined in Fig. 9. Also, a correlation of 0.36 is found between this V850 PC1 and NGP precipitation. This 1988 is considered a dry year for the Northern Great Plains as identified by the time in Figure 2b; Figure S5: Longitudinal-time Hovmoller diagram of Climate Precipitation Center (CPC) precipitation averaged among 37ºN and 43ºN (in shaded is the same precipitation plot as in Fig. 3). The superimposed black line is the CPC observed precipitation average over the region 37º-43ºN; 102º-90ºW. The superimposed red and blue lines are precipitation average over the same as the black line, but for Climate Forecast System (CFS) reforecast simulations starting in Jul 5 (red line) and Jul 10 (blue line); Figure S6: Hovmoller spatiotemporal variability of a reconstructed 200-mb geopotential height anomaly (ΔHGT). (a) Using the second Empirical Orthogonal Function (EOF2) mode. The superimposed green line is the PC2 associated with this mode. (b) Using the EOF1 mode with original NARR HGT data previously filtered with a 10- to 60-day band-pass filter. (c) Using the EOF1 mode 1 (also previously filtered with a 10- to 60-day band-pass filter) from the Climate Forecast System reforecast (CFS-R). Boxes represent the region of correlation analysis; Table S1: List of acronyms.

Author Contributions

Conceptualization, C-M.C. and F.M-A.; methodology, C-M.C. and F.M-A.; software, C-M.C. and F.M-A.; validation, C-M.C. and F.M-A.; formal analysis, C-M.C. and F.M-A.; investigation, C-M.C. and F.M-A.; resources, F.M-A.; data curation, C-M.C.; writing—original draft preparation, C-M.C. and F.M-A.; writing—review and editing, C-M.C., F.M-A., and L.C.; visualization, C-M.C.; supervision, C-M.C. and F.M-A.; project administration, F.M-A.; funding acquisition, F.M-A. All authors have read and agreed to the published version of the manuscript.

Funding

U.S. Department of Agriculture (USDA) Agriculture and Food Research Initiative Grant number NEB-21-176 and NEB-21-166 from the National Institute of Food and Agriculture, Plant Health and Production and Plant Products: Plant Breeding for Agricultural Production. the U.S. Geological Survey (USGS), the Daugherty Water for Food Global Institute (DWFI) at the University of Nebraska-Lincoln (UNL), and the UNL’s Layman Award.

Informed Consent Statement

Not applicable.

Data Availability Statement

All data sources are cited through the text and listed in the References section. Additional data can be found at https://zenodo.org/records/5784508 [61] (“Precipitation, low-level jet, and geopotential height data for analyzing sources of predictability in the US northern Great Plains: DOI 10.5281/zenodo.5784508.”).

Acknowledgments

We thank the U.S. Department of Agriculture (USDA) Agriculture and Food Research Initiative Grant number NEB-21-176 and NEB-21-166 from the National Institute of Food and Agriculture, Plant Health and Production and Plant Products: Plant Breeding for Agricultural Production; the U.S. Geological Survey (USGS), the Daugherty Water for Food Global Institute (DWFI) at the University of Nebraska-Lincoln (UNL), and the UNL’s Layman Award. Also, we are grateful with the Earth System Research Laboratory at NOAA for providing the gridded data. Also, the Climate Forecast System (CFS) retrospective reanalysis and reforecast dataset was obtained from the National Centers for Environmental Prediction (NCEP). We are grateful to the UNL Holland Computer Center for access to their high-computing facilities to perform the analysis, which code is at http://bit.ly/GP-LLJ.

Conflicts of Interest

The authors declare no conflict of interest.

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Figure 1. Summer precipitation anomaly (ΔP) of the 1993 July–August (JA) season. Precipitation units are in mm/day and the climatology is used from the 1950-2014 period. The dataset is from [23] Livneh et al. (2013), and the box defines a region (37.5º-45ºN; 103º-90ºW) for a precipitation index used in the next figures.
Figure 1. Summer precipitation anomaly (ΔP) of the 1993 July–August (JA) season. Precipitation units are in mm/day and the climatology is used from the 1950-2014 period. The dataset is from [23] Livneh et al. (2013), and the box defines a region (37.5º-45ºN; 103º-90ºW) for a precipitation index used in the next figures.
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Figure 2. (a) Precipitation climatology (P) in bars for the Northern Great Plains-Midwest region (MW=37.5º-45ºN; 103º-90ºW). The precipitation associated with the 1993 flood and 1988 drought are shown as a black line to illustrate the monthly changes in comparison with the 1981-2010 climatology. (b) Interannual variability of late spring- early summer (May through August) precipitation over the Northern Great Plains – Midwest region (37.5-45N; 103-90W). The 1993 historical flood event is highlighted as well as other major wet (red arrows) and dry (dark blue) years since 1950. The dataset is from [23].
Figure 2. (a) Precipitation climatology (P) in bars for the Northern Great Plains-Midwest region (MW=37.5º-45ºN; 103º-90ºW). The precipitation associated with the 1993 flood and 1988 drought are shown as a black line to illustrate the monthly changes in comparison with the 1981-2010 climatology. (b) Interannual variability of late spring- early summer (May through August) precipitation over the Northern Great Plains – Midwest region (37.5-45N; 103-90W). The 1993 historical flood event is highlighted as well as other major wet (red arrows) and dry (dark blue) years since 1950. The dataset is from [23].
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Figure 3. (a) Spatial Empirical Orthogonal Function (EOF1) pattern of 900-mb meridional wind from the North American Regional Reanalysis (NARR) obtained from daily fields from May 1 through September 1, 1993, with explained variance of 30%. (b) Spatial correlation patterns among the temporal Principal Component (PC1; from top figure) and both daily precipitation and (c) daily 200-mb geopotential height (HGT). Oblique lines represent significant values at the t-test 95% level of confidence.
Figure 3. (a) Spatial Empirical Orthogonal Function (EOF1) pattern of 900-mb meridional wind from the North American Regional Reanalysis (NARR) obtained from daily fields from May 1 through September 1, 1993, with explained variance of 30%. (b) Spatial correlation patterns among the temporal Principal Component (PC1; from top figure) and both daily precipitation and (c) daily 200-mb geopotential height (HGT). Oblique lines represent significant values at the t-test 95% level of confidence.
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Figure 4. Spatial pattern of the Empirical Orthogonal Function mode 2 (EOF2) from 200-mb geopotential height anomalies (ΔHGT) from the North America Regional Reanalysis (NARR) obtained from daily fields from May 1 through September 1 (MJJA), 1993, with explained variance of 11%.
Figure 4. Spatial pattern of the Empirical Orthogonal Function mode 2 (EOF2) from 200-mb geopotential height anomalies (ΔHGT) from the North America Regional Reanalysis (NARR) obtained from daily fields from May 1 through September 1 (MJJA), 1993, with explained variance of 11%.
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Figure 5. Longitudinal-time Hovmoller diagram of observed precipitation for the 1993 summer season. The latitudinal average is taken over 40ºN-50ºN. Superimposed solid lines are GP-LLJ index (magenta) and CGT index (green) obtained using Empirical Orthogonal Function analysis using the North American Regional Reanalysis (NARR). Big arrows and horizontal lines are added to indicate the cases of high CFS precipitation correlation.
Figure 5. Longitudinal-time Hovmoller diagram of observed precipitation for the 1993 summer season. The latitudinal average is taken over 40ºN-50ºN. Superimposed solid lines are GP-LLJ index (magenta) and CGT index (green) obtained using Empirical Orthogonal Function analysis using the North American Regional Reanalysis (NARR). Big arrows and horizontal lines are added to indicate the cases of high CFS precipitation correlation.
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Figure 6. Spatial patterns of the two dominant Empirical Orthogonal Functions (EOF1 and EOF2) of 900-mb meridional wind for (A) the North American Regional Reanalysis (NARR), and (B) the Climate Forecast System Retrospective Reanalysis (CFS-RR). Both obtained from the periods 1979-2014 and 1979-2010. The explained variance of these EOFs is shown at the top of each graph in percentage.
Figure 6. Spatial patterns of the two dominant Empirical Orthogonal Functions (EOF1 and EOF2) of 900-mb meridional wind for (A) the North American Regional Reanalysis (NARR), and (B) the Climate Forecast System Retrospective Reanalysis (CFS-RR). Both obtained from the periods 1979-2014 and 1979-2010. The explained variance of these EOFs is shown at the top of each graph in percentage.
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Figure 7. Unconditional probability density functions (PDF) of the correlation values for the three indices: NPG precipitation (A), GP-LLJ index (B), and CGT index (C)—cyan bars. The total number of cases for each distribution is 701; and the continues line is the fitted normal PDF. The x-axis represents the correlation values between the observation and reanalysis and the forecasted valued from CFS-R for each index, respectively. The null distribution (gray bars) is constructed by bootstrap of this pool of cases and with a randomization of the original time series before computing the correlation.
Figure 7. Unconditional probability density functions (PDF) of the correlation values for the three indices: NPG precipitation (A), GP-LLJ index (B), and CGT index (C)—cyan bars. The total number of cases for each distribution is 701; and the continues line is the fitted normal PDF. The x-axis represents the correlation values between the observation and reanalysis and the forecasted valued from CFS-R for each index, respectively. The null distribution (gray bars) is constructed by bootstrap of this pool of cases and with a randomization of the original time series before computing the correlation.
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Figure 8. Conditional bi-dimensional probability distribution (2D-PDF) constructed with equation 2 for two pair of datasets: (A) the GP-LLJ and NGP precipitation; and (B) the CGT index and NGP precipitation (Z200, PREC). The data used represents the total available cases between 1982 and 2009 (701 cases).
Figure 8. Conditional bi-dimensional probability distribution (2D-PDF) constructed with equation 2 for two pair of datasets: (A) the GP-LLJ and NGP precipitation; and (B) the CGT index and NGP precipitation (Z200, PREC). The data used represents the total available cases between 1982 and 2009 (701 cases).
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Figure 9. The conditional and unconditional probability distribution of correlation for the NGP precipitation. The x-axis is the precipitation correlation values between observation and CFS-R for the period 1982-2009 based on 701 cases. The unconditional distribution is one-dimensional PDF and is the same as in Fig S5a; here is added for comparison. The conditional distribution is based on the simultaneous occurrence of GP-LLJ and CGT threshold, computed with equation 2 in the text. The conditional probability is plotted for this condition: [GP-LLJ index]r (NARR, CFS-R) > 0.4 and [CGT index]r (NARR, CFS-R) >0.4.
Figure 9. The conditional and unconditional probability distribution of correlation for the NGP precipitation. The x-axis is the precipitation correlation values between observation and CFS-R for the period 1982-2009 based on 701 cases. The unconditional distribution is one-dimensional PDF and is the same as in Fig S5a; here is added for comparison. The conditional distribution is based on the simultaneous occurrence of GP-LLJ and CGT threshold, computed with equation 2 in the text. The conditional probability is plotted for this condition: [GP-LLJ index]r (NARR, CFS-R) > 0.4 and [CGT index]r (NARR, CFS-R) >0.4.
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Figure 10. Thirty-day Pearson temporal correlation between observed precipitation and the Climate Forecast System reforecast (CFS-R) precipitation for an area average over the Northern Great Plains (37.5°-45°N; 103°-90°W) described by bocks in two colors. The light-blue blocks represent statistically significant correlations higher than 0.35 but lower than 0.5, and the dark-blue blocks correlate higher than 0.5. Unfilled spaces have a correlation value lower than 0.35. The location of the block defines the initialization of the CFS-R. The season of analysis is from May 1 through September 1 from 1982-2009.
Figure 10. Thirty-day Pearson temporal correlation between observed precipitation and the Climate Forecast System reforecast (CFS-R) precipitation for an area average over the Northern Great Plains (37.5°-45°N; 103°-90°W) described by bocks in two colors. The light-blue blocks represent statistically significant correlations higher than 0.35 but lower than 0.5, and the dark-blue blocks correlate higher than 0.5. Unfilled spaces have a correlation value lower than 0.35. The location of the block defines the initialization of the CFS-R. The season of analysis is from May 1 through September 1 from 1982-2009.
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Figure 11. As in Figure 10, for Great Plains low-level jet (GP-LLJ) index correlation between the North American Regional Reanalysis (NARR) and the Climate Forecasting System reforecast (CFS-R) simulations for 1982-2009. (a) Correlations are shown only for the precipitation cases that are statistically significant, as defined in Figure 10. These correlations are noted in this plot with the same light-blue and dark-blue blocks when the LLJ correlation is not significant. Statistically significant correlations are classified in four groups using the following ranges: 0.35, 0.45, 0.55, and 0.65 in orange tones. Only cases from May 1 through July 31 were analyzed. (b) Correlation for the 200-mb geopotential height index (Z200) between the North American Regional Reanalysis (NARR) and Climate Forecasting System (CFS) simulations.
Figure 11. As in Figure 10, for Great Plains low-level jet (GP-LLJ) index correlation between the North American Regional Reanalysis (NARR) and the Climate Forecasting System reforecast (CFS-R) simulations for 1982-2009. (a) Correlations are shown only for the precipitation cases that are statistically significant, as defined in Figure 10. These correlations are noted in this plot with the same light-blue and dark-blue blocks when the LLJ correlation is not significant. Statistically significant correlations are classified in four groups using the following ranges: 0.35, 0.45, 0.55, and 0.65 in orange tones. Only cases from May 1 through July 31 were analyzed. (b) Correlation for the 200-mb geopotential height index (Z200) between the North American Regional Reanalysis (NARR) and Climate Forecasting System (CFS) simulations.
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Table 1. The Pearson correlation for the precipitation index (NGP precipitation), the Great Plains low-level jet (GP-LLJ) index, and the circumglobal teleconnection (CGT) index between the Climate Forecast System reforecast (CFS-R) and the North American Regional Reanalysis (NARR) for 30- day of simulations. The initial simulation time is indicated in the first column, and statistically significant results (p < 0.05) are bolded. The correlation values were aggregated for 100º-60ºW region, as observed in Figure S6.
Table 1. The Pearson correlation for the precipitation index (NGP precipitation), the Great Plains low-level jet (GP-LLJ) index, and the circumglobal teleconnection (CGT) index between the Climate Forecast System reforecast (CFS-R) and the North American Regional Reanalysis (NARR) for 30- day of simulations. The initial simulation time is indicated in the first column, and statistically significant results (p < 0.05) are bolded. The correlation values were aggregated for 100º-60ºW region, as observed in Figure S6.
Model Initialization NGP precipitation GP-LLJ index CGT index
1988.05.11 0.44 0.14 0.12
1988.05.21 0.77 0.36 0.13
1988.06.25 0.46 0.21 0.31
1988.06.30 0.37 0.39 0.57
1988.07.15 0.36 0.38 -0.33
1988.08.09 0.42 0.36 -0.39
1993.07.05 0.38 0.71 0.12
1993.07.20 0.48 0.60 0.3
1993.08.09 0.55 0.56 -0.22
1993.08.14 0.38 0.57 0.29
1993.08.24 0.45 0.01 0.12
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